Attachment 3 to the

SETTLEMENT AGREEMENT AMONG THE UNITED STATES OF AMERICA, TAOS PUEBLO, THE STATE OF NEW MEXICO, THE TAOS VALLEY ACEQUIA

ASSOCIATION AND ITS 55 MEMBER ACEQUIAS, THE TOWN OF TAOS, EL PRADO WATER AND SANITATION DISTRICT, AND THE 12 TAOS AREA MUTUAL DOMESTIC

WATER CONSUMERS’ ASSOCIATIONS

Part I: Documentation of OSE Taos Area Calibrated Groundwater Flow Model T17.0, January 11, 2006, by Peggy Barroll, PhD and Peter Burck, CGWP, NMOSE. 37 pages, plus Appendices A, B and C.

Part II: Development of the T17sup.M7 Superposition Version of the Taos Area Groundwater Model, and Water Rights Administration under the Taos (Abeyta) Settlement; April 16, 2012. by Peggy Barroll, PhD, NM OSE. 17 pages, plus Appendices A, B, C, D and E.

Attachment 3Part I

Documentation of OSE Taos Area Calibrated Groundwater Flow Model T17.0, January 11, 2006,

by Peggy Barroll, PhD and Peter Burck, CGWP, NMOSE. 37 pages, plux Appendices A, B and C.

DOCUMENTATION OF OSE TAOS AREA

CALIBRATED GROUNDWATER FLOW MODEL T17.0 1/11/2006

by

Peggy Barroll, Ph.D. and Peter Burck, CGWP New Mexico Office of the State Engineer

with

Taos Area Hydrogeologic Framework Discussion and Attachment by

Paul Drakos, Jay Lazarus, Mustafa Chudnoff and Meghan Hodgins of Glorieta Geoscience Inc.

Prepared by the New Mexico Office of the State Engineer

Water Resource Allocation Program Technical Services Division

ii

TABLE OF CONTENTS Page

Executive Summary ………………………………………………………….. 1

1 Introduction …………………………………………………………………. 1

1.1 Project Overview ……………………………………….……..…. 1

1.2 Code and Software ……………………………………………… 4

1.3 Modeled Area …………………………………………………..… 4

1.4 Conceptual Model …………………………………………….… 4

1.5 Stream-Aquifer Interaction …………………………………….. 6

1.6 Hydrogeology ……………………………………………………. 7

2 Groundwater Model Design and Input Parameters …………………... 9

2.1 Model Temporal Discretization ………………………………… 9

2.2 Model Structure …………………………………………………. 9

2.3 Areal Recharge and Mountain Front Recharge ……………… 11

2.4 Irrigation Return Flows …………………………………………. 12

2.5 Surface Water Features ………………………………………... 13

2.6 Evapotranspiration ………………………………………………. 14

2.7 Groundwater Diversions ………………………………………… 15

2.8 Hydraulic Properties ……………………………………………... 16

3 Model Calibration …………………………………………………………. 18

3.1 Calibration Overview …………………………………………….. 18

3.2 Calibration Targets ………………………………………………. 18

3.3 Calibration Results ………………………………………………. 19

4 Summary and Conclusions……………………………………………… 22

5 References…………………………………………………….…………. 23

Figures ………………….……………………………………………………. 28-37

Appendix A: Water Level Data for Calibration

Appendix B: Distribution of Hydraulic Properties, Stresses and Calibration Results

Appendix C: Hydrologic Characteristic of Basin-Fill Aquifers in the Southern San Luis Basin, New Mexico by Paul Drakos, Jay Lazarus, Bill White, Chris Banet, Meghan Hodgins, Jim Riesterer and John Sandoval, 2004.

Appendix D: CD with T17.0 Model Input Files: Calibrated Model and Future Projection Input Files.

iii

LIST OF FIGURES

Figures follow text: pages 28-37 Figure 1 Location map Figure 2 Observed water-level contour map (after Spiegel and Couse, 1969; and

Purtymun, 1969), with new exploration wells posted. Figure 3 Model grid and selected model boundary features superimposed on base

map. Figure 4 Model grid, selected model features with information on upper-most active

model layer, and stream reach identifiers. Figure 5 Schematic cross section of the Taos Valley showing geological layers

represented in the Taos Groundwater model. Figure 6 Cross-section, to scale, but with vertical exaggeration, showing model

layers with topography and water table superimposed. Figure 7 Enlarged cross-section, to scale, but with vertical exaggeration, showing

model layers with topography and water table superimposed. Enlarged to show uppermost layers in more detail.

Figure 8 Calibration Results for Taos Groundwater Model: All head observations

plotted vs. simulated heads. A perfect model would have all points landing on the 1:1 line (shown).

Figure 9 Calibration Results for Taos Groundwater Model: Frequency Distribution

of Residuals: Residual = observed head minus simulated head. Figure 10 Diagram of Model Grid with Vertical Hydrologic Gradient Sites.

iv

LIST OF TABLES

Table Page

Table 1 Participating Member of Taos Technical Committee 2

Table 2 Model Layer Descriptions…………………………………………… 10

Table 3 Transmissivity and Storage Values from Pumping Tests ……… 17

Table 4 Model Calibration Statistics………………………………………… 20

Table 5

Vertical Head Differences between Shallow and Deep Wells: Observed and Simulated…………………………………………….

21

Table 6 Model Water Budget………………………………………………… 22

1

EXECUTIVE SUMMARY

A calibrated groundwater model has been developed for the Taos Valley. This

model is the result of several years of collaboration between the NM Office of the State

Engineer, the U.S. Bureau of Reclamation, and other professional hydrologists with

considerable experience in the Taos Valley, representing the Parties to the Abeyta

Adjudication Settlement negotiations. The model was developed in response to 1) a

need for a tool to evaluate the effects of groundwater development proposed during

Adjudication Settlement Negotiations, especially groundwater diversions from deep

levels of the aquifer system, and 2) a need for a tool to administer the wells subject to

the Settlement Agreement.

Given the hydrogeologic complexity of the Taos area, this groundwater flow

model does a relatively good job matching observed water levels, the discharge from

the springs at Buffalo Pasture, and the observed large downward vertical gradients.

Simulation of the large vertical gradients constrains model vertical anisotropy, and

allows the model to simulate the interaction between the deep and shallow aquifer

systems with reasonable reliability. The model was designed, in part, to evaluate the

hydrologic effects of wells proposed under the Taos Adjudication settlement, and it is

recommended that the model be used in evaluating the hydrologic impacts of those

wells. Determination of how and whether the model should be applied to the hydrologic

evaluation of other wells should be made on a case-by-case basis.

1. INTRODUCTION 1.1 Project Overview

At the request of the Parties to the Abeyta Adjudication Settlement negotiations,

the New Mexico Office of the State Engineer (OSE) Hydrology Bureau developed a

regional, 7-layer, groundwater flow model of the Taos Valley, New Mexico using the

USGS groundwater flow simulator MODFLOW-2000. The OSE developed the model

with input from members of the Taos Technical Committee. (Table 1) The Taos

Technical Committee is comprised of geohydrologists representing the major parties

involved in Taos Settlement negotiations (State of New Mexico ex rel. State Engineer v.

2

Abeyta and State of New Mexico ex rel. State Engineer v. Arellano, Civil Nos. 7896-BB and

7939-BB (consolidated) (“Abeyta”)). Numerous model versions were generated during

this process. This report documents the version released in 2004 as version T17.0,

which was adopted by the Parties to the settlement negotiations for the purpose of

evaluating hydrologic aspects of the Settlement Agreement.

Table 1 Participating Members of Taos Technical Committee Names From Party Represented Peggy Barroll Peter Burck

NM Office of the State Engineer (OSE)

State of New Mexico

Robert Talbot Tom Bellinger

US Bureau of Reclamation (USBOR)

United States

Lee Wilson Roger Miller

Lee Wilson and Associates Taos Pueblo

Mustafa Chudnoff Jay Lazarus Meghan Hodgins Paul Drakos

Glorieta Geoscience

Town of Taos

John Shomaker John Shomaker and Associates, Inc.

Taos Valley Acequia Association

Maryann Wasiolek Michael Spinks

Hydroscience Associates Inc. El Prado Water and Sanitation District

Chris Banet Bill White John Sandoval

US Bureau of Indian Affairs (USBIA)

Taos Pueblo

This model incorporates results from recent hydrogeologic investigations,

including a recent Town of Taos/Taos Pueblo cooperative deep drilling and hydrologic

testing project sponsored by the USBOR. The geologic and hydrogeologic framework

and aquifer coefficients used in the model are presented in Drakos et al. (2004c), which

summarizes and interprets results from the deep drilling program and other Taos Valley

geologic and hydrologic investigations. The Drakos Report is presented in Appendix C

of this report. The model also incorporates the most recent geologic/hydrologic mapping

by the New Mexico Bureau of Geology and Mineral Resources. Water level data

collected by many agencies and consultants were used as calibration targets, including

new data from the deep drilling project that allowed quantification of the large vertical

hydraulic gradients present in the valley.

The model simulates groundwater flow in about 3000 feet of alluvial and volcanic

materials. Geologic strata represented in the model include Quaternary alluvial fan

3

deposits, Tertiary Servilleta basalt flows, and Tertiary Santa Fe Group sediments. Key

hydrologic processes are simulated, including natural recharge, irrigation seepage,

evapotranspiration, and the interaction between groundwater and surface water

features including the Rio Grande, its tributaries, and Buffalo Pasture springs.

The groundwater model is designed to calculate the effects of groundwater

diversions on aquifer water levels and depletion to the Rio Grande, its tributaries and

springs, including the Buffalo Pasture springs on Taos Pueblo. The tributaries supply

water for irrigation to Taos Pueblo and to members of the Taos Valley Acequia

Association. The Buffalo Pasture springs have great cultural significance to Taos

Pueblo, and the Pueblo places a high value on protecting these springs.

The groundwater model can be and has been used to evaluate scenarios in

settlement negotiations in the on-going Abeyta water rights adjudication. In addition, it

is anticipated that the model will form the basis of an administrative tool that will be

used, as appropriate on a case-by-case basis, to administer water rights and evaluate

the hydrologic impacts of proposed groundwater diversions, especially deep

groundwater diversion such as the wells proposed in the Taos Settlement Agreement as

of October 2005. (It may be preferable to use other methods to evaluate the effects of

shallow wells).

The model was run in steady state mode using long-term average stress inputs,

and calibrated to the measured water levels from area wells and groundwater discharge

estimated to occur to the Rio Grande and Buffalo Pasture. The calibrated model

simulates observed heads and groundwater discharges reasonably well, and captures

major groundwater features such as large downward vertical gradients, thus allowing

the interaction of the shallow and deep aquifer systems to be well simulated. Transient

calibration runs were made using historical metered and estimated groundwater

diversions. These transient runs gave reasonable results, but groundwater development

in the area has so far been very limited, and the available data do not show any

significant aquifer response to groundwater development.

This model was developed in conjunction with a surface water model of the Taos

Valley that was produced by the USBOR. The development of the surface water model

assisted in the development of some groundwater model input parameters, such as

irrigation return flow and evapotranspiration by riparian and wetlands vegetation.

4

However, now that these basic inputs have been developed, no other data from the

surface water model are required in order to evaluate groundwater diversions. The

groundwater model can be run independently of the surface water model in the

evaluation of development alternatives.

1.2 Code and Software The model was constructed using the modular three-dimensional finite-difference

groundwater flow code developed by the United States Geological Survey (USGS)

commonly known as MODFLOW (McDonald and Harbaugh, 1988, and Harbaugh and

McDonald, 1996). MODFLOW-2000 was used in this application (Harbaugh et al.,

2000; Hill et al., 2000). The model uses days (d) for the time unit, and the length units

are in feet (ft). Thus, head measurements are given in feet above mean sea level

(amsl), transmissivity values are in feet squared per day (ft2/d), and flow values are

reported in cubic feet per day (ft3/d).

1.3 Modeled Area

This model simulates the alluvial/volcanic aquifer system within the Taos Valley

in Northern New Mexico (Figure 1). A detailed description of the model structure is

presented in Section 2.2. The model is bounded by the mountain-front of the Sangre de

Cristo Mountains on the east, the Rio Grande on the west, and the Rio Hondo on the

north. The southern boundary is defined by the foothills of the Picuris Mountains and the

confluence of the Rio Grande and Rio Pueblo de Taos (Figure 2). The model area

includes the areas in and near the Town of Taos, Taos Pueblo, and surrounding

communities (e.g., Ranchos de Taos, Los Cordovas, Cañon, Talpa, El Prado, Arroyo

Seco, and Arroyo Hondo). The model grid is shown in Figure 3 and 4.

1.4 Conceptual Model

The Taos Valley surface water system (Figure 2) consists of the Rio Grande and

a number of tributaries that rise in the Sangre de Cristo Mountains and discharge into

the Rio Grande. These tributaries include, from north to south, the Rio Hondo, Arroyo

Seco, Rio Lucero, Rio Pueblo de Taos, Rio Fernando, Rio Chiquito and Rio Grande del

5

Rancho. The Rio Grande is deeply incised into the Servilleta basalts at the bottom of

the Taos Gorge, and the tributaries generally become more deeply incised close to their

confluence with the Rio Grande.

Recharge enters the Taos groundwater system from 1) precipitation in the

Sangre de Cristo Mountains, 2) seepage of tributary flow, 3) local precipitation, and 4)

return flow and seepage from surface water irrigation. In general, groundwater in the

shallow combined Servilleta/alluvial aquifer system flows in a southwesterly direction

from the Sangre de Cristo mountain-front, subsequently discharging into the Rio Grande

(Drakos et al. 2004c Figure 5). Based on limited data available from 12 deep wells

(Drakos et al 2004c Figure 6), groundwater in the deeper alluvial aquifer, below the

Servilleta basalts, appears to flow from east to west. Water leaves the aquifer via

discharge to surface water features, pumping, and evapotranspiration. There may be

some underflow components to and from adjacent basins, but these are not well

quantified, and have been neglected in the current analysis. A schematic cross-section

of the Taos Valley showing geologic layers represented in the model is presented in

Figure 5.

The model area includes a shallow unconfined alluvial aquifer system in the

eastern part of the Taos Valley, underlain by layers of Servilleta basalt that extend

westward to the Rio Grande. Below the Servilleta basalts, a deep aquifer system

consisting of older Santa Fe Group basin fill deposits extends to depths greater than

3000 feet. Large downward gradients are observed between the shallow and deep

systems, reflecting the drainage of groundwater from the shallow aquifer system

downward into the deep aquifer. Within the deep system itself, piezometer data from the

deep drilling project indicates moderate vertical gradients, mostly downward, but data

from two sites indicates modest upward gradients (Drakos et al., 2004c).

Groundwater development in the Taos Valley has been minor. On the order

2,500 acre-feet per year (AF/yr) of groundwater is diverted from wells, and the available

water level data do not shown any significant or regional drawdown in response to this

diversion. The few wells for which more than one water level is available do not show

any systematic response to regional pumping, but rather, water level variations appear

to reflect seasonal changes in conditions (USBIA wells near the Buffalo Pasture), or the

difference in recharge between wet and dry years.

6

A number of springs discharge groundwater in the upper Taos Valley (within a

few miles of the mountain front, where the water table is relatively shallow). The most

significant of these are associated with the Buffalo Pasture on Taos Pueblo. Much of

the spring discharge in the Taos valley appears to represent reappearing surface water

that had seeped into the ground upstream of the springs, from streams, acequias or

applied irrigation water.

Evapotranspiration from phreatophytic vegetation and wetlands consumes water

in some parts of Taos Valley, most significantly in the vicinity of the Buffalo Pasture.

Evapotranspiration along the edges of streams probably intercepts infiltrating surface

water before it could reach the regional water table, whereas wetlands farther away

from streams are assumed to directly deplete shallow groundwater.

1.5 Stream-Aquifer Interaction

The Rio Grande gains water throughout the river reach downstream of the Rio

Hondo to the confluence of the Rio Grande and the Rio Pueblo de Taos, and acts as a

drain to the groundwater system. Gains from groundwater seepage to the Rio Grande

include subsurface gains along the riverbed and gains from springs in the canyon walls.

Seepage studies and evaluation of gage data indicate that this reach gains about 20 to

25 cubic feet per second from groundwater (cfs) (Tetra Tech, 2003). The Rio Grande in

this reach also gains water from surface inflows from the Rio Hondo and the Rio Pueblo

de Taos.

The tributary streams in the Taos area vary in how well they are connected to the

groundwater system. The upper Rio Pueblo de Taos, near Taos Pueblo, is known to

gain water from the groundwater system, as do various sub-reaches of the Rio Pueblo

and Rio Lucero (USBOR, 2002). These reaches are clearly connected to the shallow

groundwater system, and groundwater pumping could intercept water that otherwise

would have discharged into these reaches. Other tributary reaches are unlikely to be

well connected to the groundwater system. Except in its uppermost reaches at or near

the mountain front, Arroyo Seco is a losing stream that is often dry, with lengthy reaches

perched well above the water table. As a result, the connection between Arroyo Seco

and the groundwater system is limited. Similarly, Rio Lucero above the Buffalo Pasture

7

is a losing stream that appears to be perched well above the water table; therefore

groundwater pumping would not affect surface water flow in that reach. There are fewer

observational data available for other tributary reaches such as the Rio Fernando, Rio

Grande del Rancho and Rio Chiquito. It is assumed in the model that t these streams

are connected to the groundwater system.

The Buffalo Pasture itself is a large wetland located in and around the lower Rio

Lucero, upstream from its confluence with the Rio Pueblo de Taos. The Buffalo Pasture

is fed by the discharge of groundwater at numerous springs. Total groundwater

discharge from the Buffalo Pasture appears to vary, and measurements and estimates

of this discharge range from 2 to 15 cfs. In 2001, the total discharge measured from

several large springs in the Buffalo Pasture totaled 7.41 cfs (USBOR, 2001). It is likely

that much of the groundwater discharge from the Buffalo Pasture originated as seepage

from the Rio Lucero and upstream acequias and also from mountain front recharge.

The location of the springs may be geologically controlled: a low-permeability

sedimentary unit may occur close to the surface under the Buffalo Pasture, forcing

groundwater to the surface (Chris Banet, USBIA, personal communication, 8/22/2003).

1.6 Hydrogeology

The Taos region is known to have at least four discrete groundwater zones or

layers within 2500 feet below land surface. Figure 5 is a schematic cross section of the

model area. There appear to be at least two water-bearing zones within the alluvial fan

sediments above the Pliocene Servilleta basalt, one at depths approximately from 5 to

200 feet and another at depths approximately from 400 to 750 feet. Water in the fan

sediments is sometimes perched and may be widespread across the eastern part of the

valley as a result of historic irrigation practices. A third water-producing interval is

located between the Upper and Middle Servilleta basalts and is informally referred to as

the Aqua Azul Aquifer (Drakos, 2004a). The thickness of the entire Servilleta Formation

(including interbedded sediments) ranges from 0 to 650 ft (Dungan et al., 1984). The

sediments below the Servilleta are correlated with Miocene Santa Fe Group clays, silts,

sands and gravels exposed in outcrop near Pilar, NM. These materials are rift fill

sediments (Galusha and Blick, 1971) and consist of moderate to poorly sorted sands

8

with clasts of intermediate volcanic rock, quartzite, and other metamorphic rocks (Bauer

and Kelson, 1998).

Groundwater generally flows from recharge areas near the Sangre de Cristo

Mountains westward toward the Rio Grande. In the eastern part of the Valley, the water

table is well above the Servilleta basalts in shallow alluvial deposits only tens of feet

below the surface. Farther west the water table is 150 ft or deeper within the Servilleta

basalts and interbedded sediments.

These geologic units are crosscut by numerous faults, generally associated with

the development of the Rio Grande Rift. The faults generally trend north-south, and step

down toward the west. Pumping test data from wells near these faults (part of the

recent USBOR drilling program) indicate that some faults act as a partial barrier to the

flow of groundwater (Drakos et al., 2004c).

The Sangre de Cristo mountain block east of the Taos Valley has significantly

different lithologic and hydrologic properties than the shallow alluvial or deeper basin fill

aquifers. The mountain block is comprised of Paleozoic sedimentary rocks, Oligocene

intrusives, and Precambrian granites. Groundwater flow within the mountain block is

assumed to be small, and its effects are simulated in the model by a mountain front

recharge term. To the north and south, the valley is constricted by the mountains and

foothills. There may be some subsurface hydrologic connection between the Taos

Valley and other valleys along the Rio Grande to the north and south, but these

connections are poorly understood and not quantified. West of the Rio Grande, data

are sparse and the hydrology is relatively poorly understood.

9

2. GROUNDWATER MODEL DESIGN AND INPUT PARAMETERS

2.1 Model Temporal Discretization

The model was first run in steady-state mode using long-term averages of natural

recharge and irrigation related return flow, and long-term average surface inflows to

tributary streams. A 40-year transient run followed, in which the average recharge and

stream-inflows from the steady-state run were continued, with the addition of increasing

historically metered and estimated groundwater diversions.

Relatively little groundwater development has occurred in the Taos Valley and a

trend of declining water levels in response to groundwater development has not been

observed. Therefore the most important and reliable part of the calibration is the

steady-state run. The transient run was made to confirm that simulated water levels

remained relatively stable, and are consistent with historically observed water levels.

2.2 Model Structure

As shown in Figures 3 and 4, the model grid encompasses a 225-square mile

area from the Rio Grande on the west, to the Taos range of the Sangre de Cristo

Mountains on the east, and from the Rio Hondo on the north, to the confluence of the

Rio Grande with the Rio Pueblo de Taos on the south. The model area measures 15

miles by 15 miles and has 60 rows, 60 columns, and 7 layers. Rows and columns are

evenly spaced and measure 1,320 feet (1/4 of a mile) on each side. The southwest

corner of the model grid is tied to the southwest corner of Section 2 of Township 24

North, Range 11 East, New Mexico Coordinate System. The grid is oriented north-

south and east-west.

Figures 3 and 4 show the extent of the hydrologically active model cells, and

some of the model boundary conditions. Model cells located in the mountain areas to

the east and the area west of the Rio Grande are inactive. The lateral boundaries of the

model are all specified flux and no-flow boundaries. These boundaries were not

simulated as head-dependent-flux boundaries because of the lack of hydrologic

information about how, or even whether, the Taos Valley aquifers extend continuously

10

beyond the boundaries here defined, and therefore it was decided that groundwater flow

across those boundaries should be strictly limited.

Figure 5 depicts a schematic geologic cross section of the model area. Layer

descriptions and nominal thickness are given in Table 2. Figures 6 and 7 show a cross

section of the model grid itself, with the observed water table superimposed. The total

model thickness is more than 3,000 feet. Land surface elevations range from about

6,100 feet amsl in the southwest to just under 8,000 feet in the northeast. Upper layers

thin and pinch out toward the west (Figure 5, 6 and 7). Consequently, rivers and

streams cut down from higher to lower layers as they flow west. Figure 4 shows a plan

view of the model, with the uppermost active layers of the model designated by color.

For reasons of model stability, the model simulates all layers as “Type 0” layers,

in which transmissivity does not change as aquifer water levels change. MODFLOW-

2000 requires input of aquifer storativity, and for the parts of Taos model layers that are

unconfined, storativity values are set so that appropriate unconfined storages are

calculated. The assumption of constant transmissivity layers is acceptable since

historical drawdowns have been very small, and anticipated drawdowns in the shallow

unconfined system are anticipated to remain small.

Geologic deposits simulated include Quaternary alluvial fan materials derived

from the Taos Range of the Sangre de Cristo Mountains (Layers 1 through 4), Pliocene

Servilleta basalt flows and interbedded sediments (Layer 5), and Miocene Santa Fe

TABLE 2. MODEL LAYER DESCRIPTIONS

LAYER GEOLOGIC DESCRIPTION THICKNESSES

(ft)

1, 2 Youngest alluvial fan deposits derived from Sangre de Cristo Mountains. . 20, 30

3

Youngest alluvial fan deposits derived from Sangre de Cristo Mountains. (Northern Basin: Reworked alluvial fan materials)

50 (up to 700)

4

Reworked alluvial fan materials and other basin fill deposits including poorly to well sorted silts, sands, and gravels <100 to 550

5 Pliocene Servilleta basalt flows and interbedded sediments 400

6, 7

Miocene Santa Fe Group sediments composed of fluvial, eolian, and lacustrine clays, silts, sands, and gravels 500, 1700

11

Group sediments consisting of clay, silt, sand, and gravel of fluvial, aeolian, and

lacustrine origin (Layer 6 and 7).

Several mapped faults are represented using the MODFLOW horizontal flow

barrier (HFB) package. These faults – Los Cordovas, Town Yard, and other unnamed

faults – generally trend north and are typically down to the west. Two types of faults,

out of numerous mapped faults, were explicitly simulated with the MODFLOW HFB

package: 1) faults for which water level and pumping test data suggest a hydrologic

influence (Drakos, et al, 2004c) and 2) a number of other representative major faults.

The faults were simulated as less transmissive than the surrounding aquifer material,

thereby slowing the east-west flow of groundwater in the deeper layers.

2.3 Areal Recharge and Mountain Front Recharge

Areal recharge is estimated at 4% of the average annual precipitation (12.55

inches per year, Garrabrant, 1993) or 0.5 inches. Areal recharge is simulated with the

MODFLOW recharge package and is distributed uniformly over the uppermost active

cells in model layers 1 through 4, where the water table is within ~200 feet of the

surface. The total amount of areal recharge applied is 1,820 acre-feet per year. Mountain front recharge of about 5,310 acre-feet per year is applied along the

mountain front on the eastern and part of the southern boundary (see diagram in

Appendix B), through the MODFLOW WEL package, which applies specified flux

stresses to the groundwater system. The amount of mountain front recharge was

originally based on discussions with the Taos Technical Committee and water budget

calculation for the area (Keller and Blisner, 1995), and modified during calibration to

improve the agreement between simulated and observed water levels and groundwater

discharge. The final amount of mountain front recharge (5,310 acre-feet per year) is

equal to about 1.3% of the estimated average annual precipitation over the

mountainous part of the watershed, which is not inconsistent with results obtained by

the USGS using chloride mass balance methods for other watersheds in the Sandia

(0.7% to 15 %) and Sangre de Cristo (3% to 6%) Mountains (Anderholm 2001 and

1994), although it is on the low side. In comparison, surface water runoff represents

about 23% of the estimated mean annual precipitation in the mountainous part of the

12

watershed. The distribution of mountain front recharge in the model area was originally

based on a water budget study by Mike Johnson (2003) and modified during calibration.

Mountain front recharge is applied in model layers 1 through 4, at rates decreasing with

depth, to represent both infiltration of streamflow at the mountain-front, and smaller

amounts of deeper flow from the mountain-block.

2.4 Irrigation Return Flows

Irrigation return flows consist of recharge from acequia/ditch/lateral seepage and

on-farm deep percolation. The amount and distribution of the return flow referred to as

“groundwater accretions” was derived from the U.S. Bureau of Reclamation’s Taos

Valley surface water model (Bellinger, 2003). Groundwater accretions represent a

fraction of the surface water diverted for irrigation of about 12,000 acres of land

(Bellinger, 2003). The surface water model calculates groundwater accretions on a

seasonal basis for a variety of surface water reaches. These reaches were correlated

with zones of cells in the groundwater model corresponding to the locations of the

conveyances and irrigated lands. A long-term average of the groundwater accretions

from the surface water model was applied to the groundwater model, on a zone-by-zone

basis (see diagram in Appendix B).

Groundwater accretions include only the part of irrigation return flows that

actually recharge the regional aquifer. Groundwater accretions do not include excess

irrigation water that remains on the surface or that only seeps into the shallow

subsurface and quickly reappears as surface water. Such water is treated in the surface

water model as being available to downstream irrigators. The groundwater accretion

components were applied in zones defined using Geographic Information System (GIS)

coverage identifying irrigated lands. Specified flux cells in the MODFLOW WEL

package were used to simulate this process. Groundwater accretions account for a

total of about 11,910 AFY, reflecting about 1 AFY of deep percolation to the aquifer per

acre of irrigated land resulting from both canal seepage and on-farm return flows.

13

2.5 Surface Water Features

Eight river reaches are simulated in the model:

• Rio Grande

• Rio Hondo

• Arroyo Seco

• Rio Lucero

• Rio Pueblo de Taos

• Rio Fernando de Taos

• Rio Chiquito, and

• Rio Grande del Rancho.

The Rio Grande is simulated using the RIV package of MODFLOW, and the

tributaries are simulated using the STR package. The RIV package simulates head-

dependent flux to and from the groundwater from a simple surface water body. The STR

package is a more complex version of RIV that allows for some accounting of the

amount of surface water in the tributaries, and allows the tributaries to go dry when all

the surface water is lost. Long-term average annual stream flow values derived from

USGS stream gage measurements are applied to the upper end of the tributary STR

cells. Since the Rio Grande is perennial and gaining in this reach, it was decided that it

was not necessary to use the more complex STR package to simulate the Rio Grande.

The model is designed such that the various reaches incise more deeply into the

model from east to west. That is, the upper (eastern) portions of the tributaries are

simulated by cells in layers 1 through 3, farther west these tributaries drop into layers 4

and 5, and the Rio Grande itself is in layers 5 and 6.

The Buffalo Pasture springs cover a roughly 600-acre marshy area on both sides

of the Rio Lucero. These springs are represented as cells in two reaches of the Rio

Lucero using MODFLOW STR package.

Input elevations associated with all STR and RIV cells were determined from

USGS Digital Elevation Model data and from topographic maps. Conductances for

tributary STR cells were initially set assuming a vertical hydraulic conductance of about

1 ft/d, and modified slightly during calibration. Final conductance values for most of the

tributary reaches ranged from 10,000 to 50,000 ft2/d. The conductances of cells

14

representing the heart of the Buffalo Pasture were much higher in order to represent the

large area of groundwater discharge, and to simulate the observed spring discharge.

The final conductance value for cells in the heart of the Buffalo Pasture was 500,000

ft2/d. The RIV cells representing the Rio Grande were also given large conductances

(550,000 ft2/d), representing the high degree of hydrologic connection that exists

between the Rio Grande and the geologic units which discharge into it.

2.6 Evapotranspiration

Non-crop evapotranspiration (ET) is simulated with the MODFLOW ET package.

The ET package was applied to all of the uppermost active cells of the model, but an

extinction depth of 6 feet was specified, which meant that ET was only active in a limited

part of the model. In most cells, a maximum evaporation rate of 2.2 feet per year was

specified based on calculation of CIR for phreatophytes made by Brian Wilson of the

OSE (Wilson and Smith, 2004). In cells containing stream reaches, the maximum ET

rate is reduced to one-fifth of that in other cells. This reduction is made in stream cells to

account for the fact that much of the water consumed by stream-side vegetation is

probably intercepted surface water, a physical process which is accounted for in the

water budget of the USBOR surface water model.

Total ET from the groundwater model is simulated to be about 5,370 acre-feet

per year, which is a reasonable value consistent with other estimates of non-crop

evapotranspiration, but not well constrained by observational measurements. A

comparison of spatial locations of model cells experiencing ET with GIS coverage of

soggy soils/wet meadows (from the National Resources Conservation Service Soil

Survey Geographic Database, SSURGO) shows relatively good agreement between the

two1.

1 The best available information regarding locations where ET actually occurs in the field is

reportedly the SSURGO data, which shows the spatial distribution of soils that developed under anoxic

conditions because of perennial or seasonal high water levels, and also soils that occur in association

with hydric conditions on the loosely defined valley floors (Roger Miller, personal communication,

7/29/2003).

15

2.7 Groundwater Diversions

Groundwater diversions from a variety of water users are represented (see

diagrams in Appendix B). The model includes the following groundwater diversions

(with recent diversion amounts):

1) Town of Taos municipal wells (currently about 840 acre-feet per year),

2) El Prado Water and Sanitation District (64 acre-feet per year),

3) about one dozen mutual domestic water users associations (about 400 acre-

feet per year)

4) approximately 1,900 individual private domestic wells (pumping 560 acre-feet

per year),

5) multiple household domestic wells (pumping 300 acre-feet per year), and

6) commercial sanitary wells using 190 acre-feet per year.

Wells were identified from OSE records and by data provided by Taos Technical

Committee members.

Metered diversions were available for public water supply wells. Diversions for

other wells were estimated at 0.25 AFY per well for domestic wells serving single

dwellings, 3.0 AFY per well for domestic wells serving multiple dwellings, and 3.0 AFY

for wells listed in OSE records as “Sanitary” type wells.

2.8 Hydraulic Properties

The model defines zones of hydraulic conductivity (K), which are then multiplied

by layer thicknesses (b) to generate transmissivity. Model hydraulic conductivities were

in part defined based upon the results of 46 aquifer tests (Drakos et al. 2004c, Tables 1,

2, 3, 4, 5; Table 3 this report), and in part based on available lithologic data.

Adjustments were made to both K values in zones and the boundaries between zones

during calibration, while keeping model values consistent with the magnitude and trends

of the available well test data. Transmissivity (T) values from aquifer tests in the shallow

system range from 250 to 6,000 ft2/d although no values are available for the shallowest

stream-channel sediments. Transmissivity in the lower aquifer system tends to be lower,

ranging from 100 to 1,600 ft2/d.

16

The final hydraulic conductivities in the calibrated model produce T values that

are consistent in trend and magnitude with the aquifer test values (see diagrams in

Appendix B). Model hydraulic conductivities in the shallow system range from 1.0 to

90.0 ft/d, yielding T values in the range from 500 to 10,000 ft2/d. A very low K and T are

given to cells within Buffalo Pasture, representing low permeability “Marsh” sediments,

and the underlying Blueberry Hill deposit, which are thought to force groundwater to

discharge in this area (verbal communication, Chris Banet, US BIA). Model hydraulic

conductivities for the deeper layers (6 and 7) are systematically lower, ranging from 0.1

to 3.0 ft/d, yielding T values of around 200 to 400 ft2/d in the central part of the Taos

Valley, and T values between 1,000 and 2,500 ft2/d for the western and southern parts

of the deep system. The higher values of T in the western part of layers 6 and 7 are

consistent with an aquifer test from the River View Acres well of 1250 ft2/d, near the Rio

Grande, but are otherwise poorly constrained by well test data.

There are few pumping tests with observation wells in the shallow aquifer in the

Taos area. Therefore, storage values for the Taos model were based on standard

hydrologic texts (Freeze and Cherry, 1979) and other alluvial aquifer models in New

Mexico (McAda and Barroll, 2002; McAda and Wasiolek, 1988). For reasons of

stability, the model simulates all layers as “Type 0”, in which a specific storage value is

multiplied by the layer thickness. Specific storage was set so as to generate the

appropriate unconfined storage coefficient (0.15) for areas that are not confined. That

is, specific storage for each cell is set equal to 0.15 divided by the saturated thickness

of the cell. For parts of the model that are confined, the specific storage is set at 2 x

10-6 per foot, which is consistent with the theoretical storage due to the compressibility

of water with adjustment for aquifer compressibility, and consistent with other water

resource groundwater models of alluvial basins (McAda and Barroll, 2002).

There is evidence that the vertical anisotropy (the ratio of horizontal hydraulic

conductivity to vertical) is large. This evidence includes the presence of 1) large

observed vertical hydraulic gradients (up to 50 feet of head decline per 100 feet of

increasing depth), and 2) horizontal low permeability beds, including thick horizontal

basalt layers. Model anisotropy was determined during calibration, in order to accurately

simulate the observed vertical gradients, and ranges from 25:1 near the edges of

certain alluvial layers, to 1400:1 in the basalt layer.

17

Table 3 Transmissivity and Storage Values from Pumping Tests Well Name Screened Depth Transmissivity (ft2/d) Storage (unitless)

Arroyo Park Shallow 495 – 561 0.00053 Baird Joint Venture Shallow 1150 – 2308 0.001 Barranca del Pueblo Shallow 454 – 882 BOR 2A Shallow 230 Buffalo Pasture Shallow 2000 – 6300 0.003 – 0.1 Cameron Shallow 414 – 588 Ceja de Colonias Shallow 235 – 282 Cielo Azul Shallow 390 Clinic Shallow 900 Colonias Point Shallow 976 – 1497 Cooper Shallow 187 – 401 Don’s Shallow 810 Hail Creek Deep Shallow 5000 0.0063 Howell Well Shallow 4278 – 7753 Kit Carson Shallow 1069 – 1764 La Fontana Shallow 2807 – 4679 La Percha Shallow 481 – 976 Riverbend Shallow 1600 0.000085 River View Acres Shallow 1250 San Juan-Chama Shallow 400 – 468 0.00025 – 0.00027 Ski & Tennis Ranch Shallow 35 – 504 TP-2 Taos North Shallow 930 Tract A PW2 Shallow 175 El Prado Shallow+Deep 3000 Airport Deep Deep est. 250 BOR 1 (RG-73095) Deep 520 – 1400 BOR 2B Deep 260 – 290 BOR 2C Deep 370 – 1470 BOR 3 (RG-74545-EX) Deep 450 – 710 0.0005 BOR 4 Deep 121 – 334 BOR 5 Deep 110 – 119 BOR 6 Deep 270 – 800 BOR 7 Deep 109 Karavas 2 (Screen 2) Deep 90 – 200 0.0014 – 0.019 Karavas 3 Deep 100 – 210 Mariposa Deep 530 National Guard Domestic Deep 760 Rio Pueblo 2000 Deep 280 – 700 Rio Pueblo 2500 Deep 115 – 140 Taos Yard Deep 400 Tract A PW Deep 300 Tract B PW Deep 600 0.0002 Tract B PW2 Deep 220 Tract B Tip – BIA 10 Deep 275 0.001 Tract B Tip – BIA 11 Deep 310 UNM Taos Deep 176 – 706

18

3. MODEL CALIBRATION 3.1 Calibration Overview

The model was started under steady-state conditions, which represented

conditions before substantial groundwater pumping, followed by a transient historical

period simulation of 40 years during which historical groundwater diversions were

applied. The model was calibrated to observed water level data, estimated discharge

from the Buffalo Pasture springs and discharge to the Rio Grande. Calibration was

done using trial-and-error methods.

Little change in model water levels or discharges was simulated to occur during

the transient simulation in most areas of the model, which is consistent with the

available observational data. Observed well hydrographs show only climatically

induced variability, and not any trend indicative of groundwater development. Therefore,

no attempt was made to simulate the observed well hydrographs; instead the simulated

change in water levels over the transient period was checked to ensure that

unreasonably large values had not been simulated.

3.2 Calibration Targets Water level data used to calibrate the model were obtained from various sources

including:

• U.S. Geological Survey (USGS) Ground-Water Site Inventory (GWSI)

• Office of the State Engineer well records (including WATERS database)

• Bauer et al. (1999)

• Garrabrant (1993)

• Glorieta Geoscience, Inc. reports

• Lee Wilson and Associates, Inc. report (1978)

• Taos Pueblo well inventory

• Purtymun (1969)

These water level data are tabulated in Appendix A.

The range of water levels is similar to the range in land surface elevation in the

model, from about 6,100 feet amsl at the Rio Grande to nearly 8,000 feet amsl near the

mountain front. There is considerable scatter in the observed water level data, in part

because of issues of hydrogeologic complexity and the presence of large hydrologic

19

gradients, but also in part because of variable data quality. The recent USBOR drilling

program provides high quality data from a number of piezometer nests, allowing

quantification of the vertical gradient. Calibration was performed so as to match both

individual water levels and to match the overall large downward vertical gradient

between the shallow and deep aquifer systems. No attempt was made to simulate the

much smaller observed upward gradient within the deep aquifer, which is assumed to

be associated with a local geologic structure (Drakos et al., 2004c).

Additional calibration targets included groundwater discharge to the Rio Grande

within the reach simulated by the model (estimated at about 1 cfs per mile or 20 cfs),

the estimated discharge from the Buffalo Pasture (estimated at various times between 2

and 15 cfs), and the general distribution of gaining and losing reaches on the tributaries,

including some seepage loss data from the Rio Lucero and Rio Pueblo de Taos.

For convenience, water level targets and the discharge target for the Buffalo

Pasture were including in MODFLOW-2000 observation package input files.

MODFLOW-2000 automatically provided output on how well these targets were

matched, which simplified evaluation of trial-and-error calibration runs.

3.3 Calibration Results

Trial-and-error calibration resulted in a model whose hydraulic properties are

relatively consistent with observed values, and that simulates observed water levels,

vertical gradients and groundwater discharges adequately. The distribution of hydraulic

properties in the calibrated model is provided Appendix B in diagram form. The match of

simulated and observed water levels (also provided in Appendix B) is generally good,

but shows considerable scatter, which is expected considering the large amount of

scatter in the available water level data. In general, the shallow system is simulated

more closely than the deep system. Model calibration statistics are given in Table 4.

50% of simulated water levels are within 20 feet of observed values, and 82% are within

50 feet, which is acceptable given the scatter in the data and the large range of

observed water levels across the model area (1267 feet). Most large residuals are

associated with wells at the edge of the basin, or wells of suspect location or screening

(we did not attempt to eliminate such outliers). Figure 8 shows observed vs. modeled

water level elevations, and Figure 9 is a chart of the distribution of residuals. The

20

residual is the difference between the observed head and the model simulated heads at

the same locations (observed head minus model-simulated head). Ideally, for a perfect

model, all residuals would be zero. Figures 8 and 9 show a reasonable distribution of

residuals for a regional model of this complex system. Residuals are mostly of

reasonable size, and their distribution is centered on zero.

The fact that the upper model layers pinch out to the west as the water table cuts

down through the geologic section causes some anomalous conditions at the limits of

these layers. In the layers 1, 2 and 3 this is treated by increasing the vertical

conductance at the western edge of the pinching layer, thus allowing water from an

upper layer to flow westward, in accordance with the hydrologic gradient, into the next

layer. This creates minor anomalies in simulated heads, especially near the western

edge of layer 4 where simulated heads drop precipitously, creating more of a “step” than

can be observed in field data. However, observed data are sparse in this area, west of

Arroyo Seco, where the water table drops hundreds of feet below land surface as the

shallow aquifer system gives way to a deeper hydrologic system. What data there are

suggest that the shallow hydrologic system represented by model layers 1-4 may not be

in direct connection with the deeper hydrologic system represented in layers 5, 6 and 7

in this area. Without more detailed local data it probably would not be worthwhile

attempting to improve the simulation of this area.

TABLE 4. Model Calibration Statistics

PARAMETER ALL LAYERS Number of Observations 354 Residual Mean (feet) 0.95 Residual Standard Deviation (feet) 44.5 Sum of Squared Residuals (feet squared) 695,424 Absolute Residual Mean (feet) 30.0 Minimum Residual (feet) -143 Maximum Residual (feet) 229 Observed Head Range (feet) 1267 Minimum Observed Head (feet) 6452 Maximum Observed Head (feet) 7719 Std. Deviation/Head Range 3.5 % Percent of Residuals within 100’ 96 % Percent of Residuals within 50’ 82 % Percent of Residuals within 30’ 67 % Percent of Residuals within 20’ 51 % Percent of Residuals within 10’ 30 %

21

This model closely simulates the large vertical gradients observed between the

shallow (layers 1-4) and deep (layers 5-7) aquifer system in the Taos Valley. Observed

difference in water level between deep and shallow wells and /or piezometers at the

same location range from 100 to over 400 feet (the deeper well having the lower water

level), and this phenomenon was well simulated by the model (see Table 5). These

well-quantified downward vertical gradients constrained model vertical anisotropy, which

in many models is a highly uncertain and unconstrained parameter because of the lack

of definitive calibration data from multi-level piezometers.

TABLE 5. Vertical Head Difference Between Shallow and Deep Wells and Corresponding Model Layers.

All Gradients Listed Reflect Lower Heads at Deeper Depths WELL OBSERVED

(feet) SIMULATED

(feet) BOR 1/ National Guard 62 104 BOR 2 and 3 218 212 BOR 4 and 6 424 405 BOR 5 132 104 BOR 7 253 260 Cielo Azul 208 217 Grumpy 137 (?) 473 Karavas 2 and 3 255 260 L25/L27 41 46 Rio Pueblo 2500 131 117

The groundwater model also adequately simulates observed groundwater

discharge targets. Analysis of recorded flows in the Rio Grande from the confluence of

the Rio Grande and Rio Hondo to the Taos Junction stream gage shows a gain of about

20 - 25 cfs (or about 1 cfs per mile). The model simulates approximately 21 cfs

discharge from groundwater in this reach. At the Buffalo Pasture, modeled discharge

from groundwater is about 5 cfs or 3,800 acre-feet per year, compared with 2 to15 cfs

range of observed discharge (which may contain a direct surface water return

component not simulated here in the model).

In addition, other qualitative flow and discharge targets were simulated

successfully. These targets include large observed losses from the upper reach of the

Rio Lucero and gains to the upper reach of the Rio Pueblo de Taos. Arroyo Seco was

22

also correctly simulated to have large losses, and as going dry over an extended reach.

The water budget from the calibrated model at the end of the transient run is provided in

Table 6. The difference between total recharge and total discharge is less than 0.05%,

and is well within acceptable limits.

TABLE 6. Groundwater Model Water Budget, End of Simulation (Present-Day Conditions)

Recharge AF/Y Discharge AF/Y

Areal Recharge from Precipitation 1,820 Discharge at Buffalo Pasture Springs 3,960Mountain Front Recharge 5,310 Evapotranspiration 5,350Irrigation Seepage 11,910 Groundwater Pumping 2,540Tributary Recharge (to aquifer) 18,810 Discharge to Tributaries 11,420Water Released from Aquifer Storage

370 Discharge to Rio Grande 14,940

Total Recharge 38,220 Total Discharge 38,210

4. SUMMARY, CONCLUSIONS, DISCUSSION The T17.0 model is the result of several years of collaboration between the OSE,

and the US Bureau of Reclamation with input from other professional hydrologists with

considerable experience in the Taos Valley representing the Parties to the Abeyta

Adjudication Settlement negotiations. The model was developed in response to 1) a

need for a tool to evaluate the effects of groundwater development proposed during

Adjudication Settlement Negotiations, especially groundwater diversions from deep

levels of the aquifer system, and 2) a need for a tool to administer the wells subject to

the Settlement Agreement. New hydrologic data became available from a deep-drilling

program funded by the U.S. Bureau of Reclamation, which was integral to the

development of a regional model of the Taos Valley that provides reasonable and

reliable results when simulating deep-aquifer pumping.

Given the hydrogeologic complexity of the Taos area, this groundwater flow

model does a relatively good job matching observed water levels, the discharge from

the springs at Buffalo Pasture, and the observed large downward vertical gradients.

Simulation of the large vertical gradients constrains model vertical anisotropy, and

allows the model to simulate the interaction between the deep and shallow aquifer

systems with reasonable reliability. This model provides reasonable and useful

23

predictions of the impacts of proposed wells. The model was designed, in part, to

evaluate the hydrologic effects of wells proposed under the Taos Adjudication

settlement, and it is recommended that the model be used in evaluating the hydrologic

impacts of those wells. Determination of how and whether the model should be applied

the hydrologic evaluation of other wells should be made on a case-by-case basis.

5. REFERENCES

Anderholm, S.K., 1994, Groundwater Recharge near Santa Fe, North-central New

Mexico. USGS Water-Resources Investigation Report 94-4078. Anderholm, S.K., 2001, Mountain-front Recharge Along the Eastern Side of the Middle

Rio Grande Basin, Central New Mexico: USGS Water-Resources Investigations Report 00-4010.

Banet, C., USBIA, personal communication, 8/22/2003 Bauer, P.W., Johnson, P.S., and Kelson, K.I., 1999, Geology and Hydrology of the

Southern Taos Valley, Taos County, New Mexico, New Mexico Bureau of Mines and Mineral Resources, Socorro, NM.

Bauer, P., and Kelson, K., 1998, Geology of Ranchos de Taos Quadrangle, Taos

County, New Mexico: New Mexico Bureau of Mines and Mineral Resources Open-file Digital Geologic Map OF-DGM 33.

Bellinger, T.R., 2003. Taos Valley Surface Water Hydrologic Model Development and

Baseline Results. Draft USBOR Technical Report, Denver Technical Center. Burck, P., Barroll, P., Core, A. and Rappuhn, D., 2004,. Taos Regional Groundwater

Flow Model. New Mexico Geological Society Guidebook, 55th Field Conference, Geology of the Taos Region, p 433-439.

Drakos, P., Lazarus, J., Riesterer, J., White, B., Banet, C., Hodgins, M., and Sandoval,

J., 2004a. Subsurface Stratigraphy in the Southern San Luis Basin, New Mexico. New Mexico Geological Society Guidebook, 55th Field Conference, Geology of the Taos Region, p 374-382.

Drakos, P., Sims, K., Riesterer, J., Blusztajn, J., Lazarus, J., 2004b. Chemical and

Isotopic Constraints on Source-Waters and Connectivity of Basin-Fill Aquifers in the Southern San Luis Basin, New Mexico. New Mexico Geological Society Guidebook, 55th Field Conference, Geology of the Taos Region, p 405-414.

24

Drakos, P., Lazarus, J., White, B., Banet, C., Hodgins, M., Riesterer, J., and Sandoval, J., 2004c. Hydrologic Characteristics of Basin-Fill Aquifers in the Southern San Luis Basin, New Mexico. New Mexico Geological Society Guidebook, 55th Field Conference, Geology of the Taos Region, p 391-404.

Dungan, M. A., Muehlberger, W.R., Leininger, L., Peterson, C., McMillan, N.J., Gunn,

G., Lindstron, M., and Haskin, L., 1984. Volcanic and sedimentary stratigraphy of the Rio Grande gorge and the late Cenozoic geologic evolution of the southern San Luis Valley, in New Mexico Geological Society Guidebook 35th Field Conference, Rio Grande Rift: Northern New Mexico, p. 157-170.

Freeze, R.A. and Cherry, J.A., 1979. Groundwater. Prentice-Hall, Inc., Englewood Cliffs,

N.J. 604 p. Galusha, T., and Blick, J., 1971, Stratigraphy of the Santa Fe Group, New Mexico:

Bulletin of the American Museum of Natural History, v. 144, Article 1. Garrabrant, L.A., 1993, Water Resources of Taos County, New Mexico, U.S. Geological

Survey Water-Resources Investigations Report 93-4107, Albuquerque, NM. Glorieta Geoscience, Inc., June, 1991, Geohydrology of the Pinones de Taos, Taos

County, New Mexico, Consultant Report prepared for Stephen Natelson and Fred Fair, OSE file copy.

Glorieta Geoscience, Inc., March, 1995, Town of Taos San Juan/Chama Diversion

Project Phase 2, Volume 1, Production Well and Observation Well Installation, Testing, and Determination of Aquifer Coefficients, Consultant Report prepared for the Town of Taos and Lawrence Ortega & Associates, OSE file copy.

Glorieta Geoscience, Inc., August, 1997, Pumping Test Analysis, Arroyo Seco School

Well, Taos County, New Mexico, Consultant Report prepared by Paul Drakos for Fennell Drilling Co., OSE file copy.

Glorieta Geoscience, Inc., 2000, Drilling and Testing Report, Bureau of Reclamation

2000-Feet Deep Nested Piezometer/Exploratory Well (BOR #1), Taos, NM, Consultant Report prepared by Paul Drakos and Meghan Hodgins for the Town of Taos.

Glorieta Geoscience, Inc., 2002, Drilling and Testing Report, Bureau of Reclamation

2000-Feet Deep Nested Piezometer/Exploratory Well (BOR #2), and 2100-Feet Deep Production Well (BOR #3) Paseo del Ca�on West Site, Taos, NM, Consultant Report prepared by Paul Drakos and Meghan Hodgins for the Town of Taos.

Harbaugh, A.W and M.G. McDonald, 1996, User’s Documentation of MODFLOW-96, an

update to the U.S. Geological Survey Modular Finite-Difference Ground-Water Flow Model, U.S. Geological Survey Open-File Report 96-485, Reston, VA.

25

Harbaugh, A.W., Banta, E.R., Hill, M.C., and McDonald, M.G., 2000, MODFLOW-2000,

the U.S. Geological Survey modular ground-water model -- User guide to modularization concepts and the Ground-Water Flow Process: U.S. Geological Survey Open-File Report 00-92, 121 p.

Hill, M.C., Banta, E.R., Harbaugh, A.W., and Anderman, E.R., 2000, MODFLOW-2000,

the U.S. Geological Survey modular ground-water model -- User guide to the Observation, Sensitivity, and Parameter-Estimation Processes and three post-processing programs, U.S. Geological Survey Open-File Report 00-184, 210 p.

Johnson, M., 2003. “Taos Groundwater Model Recharge Study.” Internal OSE Draft

Memorandum dated June 30, 2003. Keller and Bliesner, 1995, Taos Valley Water Balance (1958 – 1988). 1 page table. McAda D.P., and Barroll, P., 2002. Simulation of Groundwater Flow in the Middle Rio

Grande Basin between Cochiti and San Acacia, New Mexico. U.S. Geological Survey Water-Resources Investigations Report 02-4200.

McAda D.P. and Wasiolek, M., 1988; Simulation of the Regional Geohydrology of the

Tesuque Aquifer System near Santa Fe, New Mexico. U.S. Geological Survey Water-Resources Investigations Report 87-4056.

McDonald, M.G. and A.W. Harbaugh, 1988, A Modular Three-Dimensional Finite-

Difference Ground-Water Flow Model, Techniques of Water Resources Investigations of the United States Geological Survey, Book 6, Chapter A1, USGPO, Washington, D.C.

Miller, R. Personal Communication, 7/29/2003. New Mexico Office of the State Engineer, 2000, Well Records stored in the Water

Administration Technical Engineering Resource System (WATERS) Database. Purtymun, W.D., 1969, General ground-water conditions in Taos Pueblo, Tenorio Tract,

and Taos Pueblo Tracts A and B, Taos County, New Mexico. US Department of the Interior, Geological Survey, Albuquerque, NM.

Spiegel, Z. and Couse, I.W., 1969, Availability of groundwater for supplemental

irrigation and municipal-industrial uses in the Taos Unit of the U.S. Bureau of Reclamation San-Juan Chama Project, Taos County, New Mexico. New Mexico State Engineer, Open-File Report, 22 p.

Soil Survey Staff, Natural Resources Conservation Service, United States Department

of Agriculture. Soil Survey Geographic (SSURGO) Database for Taos County and Parts of Rio Arriba and Mora Counties, New Mexico. Available URL: "http://soildatamart.nrcs.usda.gov" Accessed 2003.

26

Taos Federal Negotiation Team, undated, Hydrology and Water Management in the

Taos Basin: A Guide for Decision-Makers. (Informally known as the Taos Data Book). Prepared in cooperation with Taos Pueblo, New Mexico State Engineer Office, Taos Valley Acequia Association, Town of Taos, New Mexico.

Taos Pueblo Well Inventory, 2000. Provided by Chris Banet of the U.S. Bureau of

Indian Affairs. Tetra Tech, 2003. Rio Grande Seepage Final Study Report, Taos Box Canyon, Report.

Prepared for the U.S. Bureau of Reclamation USBR Contract No. 00-CA-30-0027, Delivery Order 00-C5-40-0027, Dated April 2003.

USBIA, 2001, U.S. Bureau of Indian Affairs, Site Completion Report for Subsurface

Drilling, Sampling, and Testing of BOR #5 at West Deep Site, Taos Pueblo, Taos County, New Mexico. Prepared by USBIA, Southwest Regional Office (SWRO), Branch of Water Rights, Geohydrology Section. Prepared for Proposal for Technical Studies Conducted to Assist Settlement Discussions in the NM v. Abeyta, Drilling Program, Pueblo Portion, October 2001.

USBIA, 2003, U.S. Bureau of Indian Affairs, BOR 4 Site Completion Report for the

Pueblo Portion at Taos Pueblo, Taos County, New Mexico. Prepared by USBIA, Southwest Regional Office (SWRO), Branch of Water Rights, Geohydrology Section. Prepared for Proposal for Technical Studies Conducted to Assist Settlement Discussions in the NM v. Abeyta, Drilling Program, Pueblo Portion, March 2003.

USBIA, 2003, U.S. Bureau of Indian Affairs, BOR 5 Site Completion Report for the

Pueblo Portion at Taos Pueblo, Taos County, New Mexico. Prepared by USBIA, Southwest Regional Office (SWRO), Branch of Water Rights, Geohydrology Section. Prepared for Proposal for Technical Studies Conducted to Assist Settlement Discussions in the NM v. Abeyta, Drilling Program, Pueblo Portion, March 2003.

USBIA, 2003, U.S. Bureau of Indian Affairs, BOR 6 Site Completion Report for the

Pueblo Portion at Taos Pueblo, Taos County, New Mexico. Prepared by USBIA, Southwest Regional Office (SWRO), Branch of Water Rights, Geohydrology Section. Prepared for Proposal for Technical Studies Conducted to Assist Settlement Discussions in the NM v. Abeyta, Drilling Program, Pueblo Portion, March 2003.

USBIA, 2003, U.S. Bureau of Indian Affairs, BOR 7 Site Completion Report for the

Pueblo Portion at Taos Pueblo, Taos County, New Mexico. Prepared by USBIA, Southwest Regional Office (SWRO), Branch of Water Rights, Geohydrology Section. Prepared for Proposal for Technical Studies Conducted to Assist Settlement Discussions in the NM v. Abeyta, Drilling Program, Pueblo Portion, March 2003.

27

USBOR, 2002. Summary of Discharge Measurements Performed on Taos Valley Streams and Canals in 1983, 1989, 2000, and 2001. Denver Technical Center, February 2002.

USGS, 2000, United States Geological Survey Ground-Water Site Inventory (USGS

GWSI). Wilson, B.C. and M. Smith, 2004, Taos Pueblo and Rio Pueblo de Taos drainage basin,

Taos County, New Mexico; Quantification of Irrigation Water Requirements. OSE Memorandum dated 2/13/2004.

Wilson, L., Anderson, S.T., Jenkins, D.N., and Lovato, P., 1978, Water availability and

water quality, Taos County, New Mexico: Consultant report prepared for the Taos County Board of Commissioners by Lee Wilson and Associates, Inc., Santa Fe, New Mexico.

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Figure 2. Observed Water Level Contour Map, contour elevations given in feet amsl (after Spiegel and Couse, 1969; and Purtymun, 1969). Also shown: locations of key wells.

29

Figure 3. Model Grid and Selected Model Boundary Features. Numbered Cells Represent MODFLOW STR Segments.

30

Diagram of STR Reach Numbers. OSE Taos Model T17.0 Uppermost Active LayerSplit between 1 and 16 designates location of last diversion on Rio Hondo 1 Reach 1 5 SimulatedSplit between 14 and 15 designates location of last diversion on Rio Pueblo de Taos Number 3 6 Faults

row 41 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50

1 2 3 4 1 1 1 1 5 16 16 16 16 1 1 1 1 1 1 1 1 6 16 16 16 16 16 16 16 16 1 1 1 1 1 1 1 1 1 1 7 16 16 8 9

10 2 2 2 2 2 2 11 2 2 12 2 2 13 2 14 2 3 3 3 15 2 2 3 3 16 2 3 17 2 3 18 2 3 19 2 3 20 2 3 21 2 3 22 2 2 3 23 2 3 24 2 3 25 2 3 26 2 3 27 2 3 28 2 3 29 2 3 30 2 3 31 2 4 4 5 32 2 4 4 5 5 7 7 7 7 33 2 4 5 5 7 34 2 2 6 5 7 35 2 6 7 36 2 2 6 6 7 37 2 9 9 7 7 7 38 2 2 9 9 39 2 9 9 40 2 2 9 41 2 9 42 2 9 9 43 2 10 9 9 8 8 8 8 8 44 2 10 10 10 8 8 8 8 45 2 10 8 8 8 46 15 14 14 14 14 14 8 47 15 15 13 8 48 15 15 13 8 49 15 13 8 50 15 15 13 13 51 15 15 13 13 52 15 15 13 53 15 15 15 13 54 15 15 13 55 15 15 13 56 15 15 15 13 13 57 15 15 13 58 15 15 12 11 59 15 12 12 11 60 15 12 12 11

column

31

Figure 5. Schematic Cross-Section of the Taos Valley Showing Geologic Layers Represented in the Taos Regional Groundwater Model. Layer Thickness information provided in Table 2.

32

Cro

ss S

ectio

n of

Mod

el L

ayer

s, O

SE T

aos

Gro

undw

ater

Mod

el T

17.0

, 200

4

3500

4000

4500

5000

5500

6000

6500

7000

7500

02

46

810

1214

Dis

tanc

e (m

iles)

Elevation (feet amsl)

Land

Sur

face

Ele

vatio

n

Wat

er T

able

(Spi

egel

and

Cou

se, 1

969)

Laye

r 7

Laye

r 6

Laye

r 5 -

Bas

altsLa

yer 4

Laye

r 1La

yer 2

Laye

r 3

Eas

t

Rio

Gra

nde

Taos

Pue

blo

33

Cro

ss S

ectio

n of

Mod

el L

ayer

s, O

SE T

aos

Gro

undw

ater

Mod

el T

17.0

, 200

4

5500

6000

6500

7000

7500

02

46

810

1214

Dis

tanc

e (m

iles)

Elevation (feet above MSL)

Land

Sur

face

Ele

vatio

n

Wat

er T

able

(Spi

egel

and

Cou

se, 1

969)

Laye

r 7Laye

r 6

Laye

r 5 -

Bas

alts

Laye

r 4

Laye

r 1La

yer 2

Laye

r 3

Rio

Gra

nde

Eas

t

Taos

Pue

blo

34

resi

dual

s-17

upda

ted.

xls

5/23

/200

5 2

:36

PM

Cal

ibra

tion

Res

ults

: Tao

s G

roun

dwat

er M

odel

ver

sion

T17

.0 1

/04

Obs

erve

d vs

. Sim

ulat

ed H

eads

All

Laye

rs

6300

6400

6500

6600

6700

6800

6900

7000

7100

7200

7300

7400

7500

7600

7700

7800

6300

6400

6500

6600

6700

6800

6900

7000

7100

7200

7300

7400

7500

7600

7700

7800

Obs

erve

d H

eads

(fee

t abo

ve m

eans

sea

leve

l)

Model Simulated Heads

35

5/23

/200

5 r

esid

uals

-17u

pdat

ed.x

ls

Cal

ibra

tion

Res

ults

Tao

s m

odel

T17

1/0

4Fr

eque

ncy

Dis

trib

utio

n of

Res

idua

lsA

neg

ativ

e re

sidu

al in

dica

tes

that

sim

ulat

ed v

alue

s ar

e to

o hi

gh

010203040506070<-100

-100 to -90

-90 to -80

-80 to -70

-70 to -60

-60 to -50

-50 to -40

-40 to -30

-30 to -20

-20 to -10

-10 to 0

0 to 10

10 to 20

20 to 30

30 to 40

40 to 50

50 to 60

60 to 70

70 to 80

80 to 90

90 to 100

>100

Ran

ge o

f Res

idua

l (ft)

Frequency

36

Location Map for Vertical Hydraulic Gradient Datamodel: columns Well Location on Model Gridrow 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50

1234 Rio Hondo56789 Arroyo Seco

101112 Cielo Azul13 Rio Lucero141516 BOR 717 Grumpy181920212223 BOR 4/BOR 6 BOR 524

252627

28293031 Buffalo Pasture

3233 Rio Pueblo34 de Taos

353637 Karavas 2/Karavas 3

38 Taos Town Wells394041 Rio L97/ L91

42 Grande43 Rio 44 Fernando

45 Taos Yard46

47 BOR 2/ BOR 348 Rio Pueblo 250049

50 L25/ L27515253 Rio Grande54 Rio Pueblo del Rancho55 de Taos5657 BOR 1/ National Guard58 Rio Chiquito5960

37

APPENDIX A

Water Level Data Used for Calibration of Taos Groundwater Model T17.0

Water level data compiled by OSE personnel from a variety of sources:

• U.S. Geological Survey (USGS) Ground-Water Site Inventory (GWSI)

(Source ID: A##)

• Office of the State Engineer Well Records (including WATERS database)

(Source ID: D##)

• Bauer et al. (1999) (Source ID: B##)

• Garrabrant (1993) (Source ID: G##)

• Glorieta Geoscience, Inc. Reports (Source ID: GG##)

• Lee Wilson and Associates, Inc. Report (1978) (Source ID: L##)

• Taos Pueblo Well Inventory (Source ID: P##)

• Purtymun (1969) (Source ID: Y##)

Well locations for many wells were derived from PLSS or other data using GIS

techniques.

Row, column and offset values designated in red were adjusted to place

observation at the center of cells located at edge of active model domain, in

order to permit MODFLOW-2000 to calculate residuals.

Row, column and offset values designated in blue were estimated based on

available PLSS data.

Appendix A page 1

Tabl

e A

1

Wel

l ID

Sour

ce ID

MO

DFL

OW

Ta

rget

ID

XU

TM

NA

D83

YU

TM

NA

D83

Mod

elLa

yer

Row

Col

Row

of

fset

Col

of

fset

Gro

und

Surf

ace

Elev

atio

n

Dep

th

to

Wat

er

Wat

er

Leve

l El

evat

ion

Tota

l D

epth

OW

-9 S

hallo

wP4

0P

4044

9210

4037

410

121

41-0

.23

0.24

7460

4074

2041

OW

-9 D

eep

P39

P39

4492

1040

3741

01

2141

-0.2

30.

2474

6048

7412

65W

est W

ell -

BIA

-19

P21

BIA

1944

7320

4036

100

124

370.

03-0

.45

7242

4571

9776

Ace

quia

Wel

l - B

IA 1

2P1

3B

IA12

4482

7040

3501

01

2739

-0.2

7-0

.09

7198

3471

6465

OW

-1P2

9P

2944

8750

4035

010

127

40-0

.27

0.10

7207

3871

6958

OW

-8P3

8O

W8

4497

5040

3461

01

2843

-0.2

7-0

.41

7215

3671

7937

MW

-2P3

0P

3044

9150

4033

970

129

410.

320.

1071

2210

7112

32R

G-2

7258

L194

L194

4473

3540

3361

51

3037

0.20

-0.4

170

935

7088

40M

W-4

P32

P32

4492

2040

3365

01

3041

0.11

0.27

7110

1670

9426

MW

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1P

3144

9350

4033

660

130

420.

09-0

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7110

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Elev

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Tao

s G

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pbar

roll

H

OB

S-7

L.xl

s lP

age

110

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2005

App

endi

x A

pag

e 2

Tabl

e A

1

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l ID

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MO

DFL

OW

Ta

rget

ID

XU

TM

NA

D83

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n

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to

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l El

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ion

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n/D

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a in

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a U

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r the

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s G

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el C

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inat

esW

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ion

Wel

l ID

RG

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App

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pag

e 10

APPENDIX B Distribution of Hydraulic Properties, Stresses and Calibration Residuals for

Taos Groundwater Model T17.0 This Appendix contains the following model information:

1) Hydraulic Conductivity (K) Diagrams, Layers 1 through 7

2) Transmissivity (T) Diagrams, Layers 1 through 7

3) Distribution of Irrigation Return Flow (Groundwater Accretions from

Irrigation)

4) Distribution of Mountain-Front Recharge

5) Table Summarizing Well Pumping Simulated in Model

6) Distribution of Municipal, Domestic and Sanitary Pumping Diagrams

7) Calibration Residuals Diagrams, Layers 1 through 7

All diagrams were generate using Microsoft Excel for illustrative purposes,

and are not to scale, and generally have some horizontal exaggeration. Model

cells are actually squares: ¼ mile by ¼ mile. Row values are listed along the left

hand side, and column values are listed along the top of each diagram.

These diagrams include a few basic model features. RIV and STR cells

that represent the Rio Grande and its tributaries are designated by bordered

cells. The Buffalo Pasture is denoted by bordered STR cells with pink font within.

The background colors of the cells indicate which layer contains the uppermost

active cell at each x, y location for the model as a whole.

• Light Blue Cells: the uppermost active cells are in layer 1.

• Yellow Cells: the uppermost active cells are in layer 3 (layers 1 and 2

are not active in these locations)

• Orange Cells: The uppermost active cells are in layer 4 (layers 1, 2

and 3 are not active in these locations)

• Green Cells: The uppermost active cells are in layer 5 (layers 1, 2, 3

and 4 are not active in these locations)

• White cells: Only the white cells representing the Rio Grande, which

are the bordered white cells along the left hand side of the active

model grid, are active. These cells are in layer 6.

Appendix B page 1

Laye

r 1 H

ydra

ulic

Con

duct

ivity

(ft/d

ay)

K1

12

34

56

78

910

1112

1314

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1920

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App

endi

x B

pag

e 5

Laye

r 5 H

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Con

duct

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(ft/d

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r 5 H

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Con

duct

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(ft/d

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11

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App

endi

x B

pag

e 6

Laye

r 6 H

ydra

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Con

duct

ivity

(ft/d

ay)

Laye

r 6 H

ydra

ulic

Con

duct

ivity

(ft/d

ay)

K6

12

34

56

78

910

1112

1314

1516

1718

1920

2122

2324

2526

2728

2930

3132

3334

3536

3738

3940

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10

00

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33

33

33

33

33

33

33

33

33

33

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0.1

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20

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33

33

33

33

33

33

33

33

33

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33

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33

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33

33

33

33

33

33

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33

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33

33

33

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33

33

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33

33

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10.

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33

33

33

33

33

33

33

33

33

33

33

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10.

10.

10.

10.

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08

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33

33

33

33

33

33

33

33

33

33

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10.

10.

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09

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00

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33

33

33

33

33

33

33

33

33

33

33

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10.

10.

10.

10.

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10.

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10.

10.

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10

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33

33

33

33

33

33

33

33

33

33

33

33

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0.1

0.1

0.1

0.1

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0.1

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33

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33

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33

33

33

33

33

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10.

10.

10.

10.

10.

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10.

10.

10.

10.

10.

10.

10.

10.

10

00

120

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33

33

33

33

33

33

33

33

33

33

33

33

33

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0.1

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0.1

0.1

0.1

0.1

0.1

0.1

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33

33

33

33

33

33

33

33

33

33

33

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10.

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10.

10.

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10.

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10.

10.

10.

10.

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10

00

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33

33

33

33

33

33

33

33

33

33

33

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10.

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10.

10.

10.

10.

10.

10.

10.

10.

10.

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33

33

33

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33

33

33

33

33

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33

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30.

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30.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

160

00

00

33

33

33

33

33

33

33

33

33

33

33

30.

30.

30.

30.

30.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

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00

33

33

33

33

33

33

33

33

33

33

33

30.

30.

30.

30.

30.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

180

00

03

33

33

33

33

33

33

33

33

33

33

33

30.

30.

30.

30.

30.

10.

10.

10.

10.

10.

10.

10.

10.

10.

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10.

10.

10.

10

00

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00

00

33

33

33

33

33

33

33

33

33

33

33

33

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

00

200

00

33

33

33

33

33

33

33

33

33

33

33

33

30.

30.

30.

30.

30.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

021

00

03

33

33

33

33

33

33

33

33

33

33

33

33

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

00

022

00

03

33

33

33

33

33

33

33

33

33

33

33

33

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

00

023

00

03

33

33

33

33

33

33

33

33

33

33

33

33

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

00

240

00

03

33

33

33

33

33

33

33

33

33

33

33

30.

30.

30.

30.

30.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

250

00

03

33

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

026

00

00

33

33

33

33

33

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

270

00

03

33

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

028

00

00

33

33

33

33

33

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

290

00

03

33

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

030

00

00

33

33

33

33

33

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

310

00

03

33

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

032

00

00

33

33

33

33

33

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

330

00

00

33

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

034

00

00

00

33

33

33

33

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

350

00

00

03

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

036

00

00

00

33

33

33

33

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

20.

20.

20.

20.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

370

00

00

03

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.2

0.2

0.2

0.2

0.2

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

038

00

00

00

33

33

33

33

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

20.

20.

20.

20.

20.

20.

10.

10.

10.

10.

10.

10.

10.

10

00

390

00

00

03

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

040

00

00

00

33

33

33

33

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

10.

10.

10.

10.

10.

10.

10.

10

00

410

00

00

03

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

00

420

00

00

03

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

00

430

00

00

33

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

0.1

0.1

00

00

044

00

00

03

33

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

0.1

0.1

00

00

045

00

00

03

33

33

33

33

33

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

50.

50.

50.

50.

50.

50.

50.

50.

50.

10.

10.

10.

10.

10.

10

00

00

460

00

00

33

33

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

0.1

00

00

00

470

00

00

33

33

33

33

33

33

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.3

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

00

00

00

048

00

00

33

33

33

33

33

33

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

30.

50.

50.

50.

50.

50.

50.

50.

50.

50.

10.

10.

10.

10

00

00

00

490

00

03

33

33

33

33

33

33

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

0.1

00

00

00

500

00

03

33

33

33

33

33

33

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

0.1

00

00

00

510

00

00

33

33

33

33

33

33

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

00

00

00

052

00

00

03

33

33

33

33

33

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

00

00

00

053

00

00

33

33

33

33

33

30.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

10.

10.

10

00

00

00

054

00

00

33

33

33

33

33

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

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0.1

0.1

00

00

00

00

550

00

03

33

33

33

33

30.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

10.

10

00

00

00

00

560

00

03

33

33

33

33

30.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50

00

00

00

00

00

570

00

33

33

33

33

33

30.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50

00

00

00

00

00

00

580

00

33

33

33

33

33

30.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50

00

00

00

00

00

00

590

00

33

33

33

33

33

30.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50

00

00

00

00

00

00

060

00

03

33

33

33

33

33

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

00

00

00

00

00

00

00

0

App

endi

x B

pag

e 7

Laye

r 7 H

ydra

ulic

Con

duct

ivity

(ft/d

ay)

Laye

r 7 H

ydra

ulic

Con

duct

ivity

(ft/d

ay)

K7

12

34

56

78

910

1112

1314

1516

1718

1920

2122

2324

2526

2728

2930

3132

3334

3536

3738

3940

4142

4344

4546

4748

4950

10

00

00

00

00

00.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

10.

10.

10.

10.

10.

10.

10

00

00

00

00

00

02

00

00

00

00

00.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

00

00

00

30

00

00

00

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

00

00

00

40

00

00

00

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

00

00

00

50

00

00

00

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

00

00

00

60

00

00

00

00.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

00

07

00

00

00

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

00

80

00

00

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

00

90

00

00

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

010

00

00

00

00.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

110

00

00

00.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

120

00

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

013

00

00

00.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

140

00

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.15

0.15

0.15

0.15

0.1

0.1

0.1

0.1

0.1

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0.1

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00

015

00

00

00.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

160

00

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

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0.5

0.15

0.15

0.15

0.15

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

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0.1

0.1

0.1

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00

017

00

00

00.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

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50.

50.

50.

150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

180

00

00.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

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50.

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50.

50.

50.

50.

50.

150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

019

00

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.15

0.15

0.15

0.15

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

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00

00

200

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

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0.5

0.5

0.5

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0.5

0.5

0.15

0.15

0.15

0.15

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

00

210

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

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0.5

0.5

0.5

0.5

0.5

0.15

0.15

0.15

0.15

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

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0.1

0.1

0.1

0.1

00

00

022

00

00.

50.

50.

50.

50.

50.

50.

50.

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50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

00

230

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.15

0.15

0.15

0.15

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

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0.1

0.1

0.1

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00

00

240

00

00.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

50.

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50.

50.

50.

50.

50.

150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

250

00

00.

50.

50.

50.

50.

50.

50.

50.

50.

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150.

150.

150.

150.

150.

150.

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150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

260

00

00.

50.

50.

50.

50.

50.

50.

50.

50.

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150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

270

00

00.

50.

50.

50.

50.

50.

50.

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50.

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150.

150.

150.

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150.

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150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

280

00

00.

50.

50.

50.

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50.

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150.

150.

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150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

290

00

00.

50.

50.

50.

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150.

150.

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150.

150.

150.

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150.

150.

150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

300

00

00.

50.

50.

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150.

150.

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150.

150.

150.

150.

150.

150.

150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

310

00

00.

50.

50.

50.

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150.

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150.

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150.

150.

150.

150.

150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

320

00

00.

50.

50.

50.

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50.

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150.

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150.

150.

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150.

150.

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150.

150.

150.

150.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10.

10

00

330

00

00

0.5

0.5

0.5

0.5

0.5

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0.15

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0.15

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0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

034

00

00

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.5

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.15

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

0.1

00

035

00

00

00

0.5

0.5

0.5

0.5

0.5

0.5

0.5

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0.5

0.15

0.15

0.15

0.15

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0.15

0.15

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0.15

0.15

0.15

0.15

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0.1

0.1

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0.1

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0.1

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0.1

0.1

00

036

00

00

00

0.5

0.5

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0.2

0.2

0.2

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0.1

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0.1

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0.1

0.1

00

037

00

00

00

0.5

0.5

0.5

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00

038

00

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00

039

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00

040

00

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00

041

00

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00

420

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00

043

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00

440

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00

00

045

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00

460

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00

00

00

470

00

00

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00

00

00

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00

00

049

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Zones of Irrigation Return Flow ApplicationAveragcolrow 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49 50

123 14 1 1 15 1 1 1 1 1 1 1 1 4 2 2 2 2 2 2 2 2 26 1 1 1 1 1 1 1 1 3 3 3 3 4 4 4 4 4 4 2 2 2 2 2 2 2 2 2 4 47 1 1 3 3 3 3 3 3 3 4 4 4 4 4 4 4 4 4 4 4 4 4 4 4 4 4 4 48 3 3 3 3 3 3 4 4 4 4 4 4 4 4 4 4 4 4 4 4 4 4 4 49 3 3 3 3 4 4 4 4 4 4 4 4 4 4 4 4 4 4 4 4 4

10 4 4 4 4 4 4 4 4 4 4 4 4 4 4 4 411 4 4 4 4 4 4 4 4 4 6 6 6 6 6 612 4 4 4 4 4 4 4 6 6 6 6 613 4 4 4 4 4 6 6 6 6 614 4 4 4 4 6 6 6 6 6 6 615 4 4 6 6 616 4 6 6 617 4 6181920212223 524 5 7

25 5 6 6 7 7 826 5 5 6 6 7 7 7 7 8 827 5 6 6 7 7 7 7 8 8

28 5 5 5 6 6 7 7 7 7 7 8 829 5 6 6 7 7 7 7 7 8 830 6 7 7 7 7 7 8 8 831 6 6 7 7 7 7 7 8 8 8 8

32 5 6 7 7 7 7 7 7 8 8 8 8 8 8 8 833 5 5 7 7 7 7 7 7 8 8 8 8 9 9 9 934 6 7 7 7 7 7 7 8 8 8 9 9 9 9 9

35 5 7 7 7 7 7 8 8 8 9 9 9 9 936 5 7 7 7 7 8 8 8 9 9 9 937 5 7 7 7 7 8 8 8 9 9

38 5 7 7 7 7 7 9 9 9 9 939 5 7 7 7 7 7 7 9 9 9 9 940 7 7 7 7 7 9 9 9 9 9 941 5 7 7 7 7 7 9 9 9 9 9 9

42 7 7 7 7 7 9 9 9 9 9 943 7 7 7 7 9 9 9 9 9 9 9 9 9 944 7 7 7 10 10 10 10 10 9 9 9 9

45 10 10 10 10 10 10 10 10 10 10 10 10 9 9 946 12 12 12 12 11 11 11 10 10 10 10 10 10 10 9 9

47 12 12 12 12 12 11 11 11 11 11 11 11 10 10 10 10 10 10 1048 12 12 12 12 12 12 12 12 11 11 11 11 11 11 10 10 10 10 1049 12 12 12 12 12 11 11 11 11 11 11 10 10 10 10

50 12 12 11 11 11 1151 12 11 11 11 11 11 1152 12 12 11 11 11 11 11 1153 12 12 11 11 11 11 1154 12 12 12 12 11 11 11 11 11 11 1155 12 12 12 12 11 11 11 11 11 11 11 1156 12 12 12 12 11 11 11 11 11 11 1157 12 12 12 12 11 11 11 11 11 1158 12 12 12 11 11 11 11 1159 11 11 11 11 1160 12 11 11 11

A - NW of Rio HondoB - NE of Rio HondoC - SW of Rio Hondo

Location Description of Zone

Application of Irrigation Return Flows to Groundwater

13

338169334

1720319424

211514831516

6789

2345

101112

D - BTW RH & ASE - West Side of ASF - South Side of AS

G - Btw AS & RLH - Btw RL & RPdT

I - Btw RPdT & RFdTJ - South Side of RFdT

K - East Side of RGdR & RCL - West Side of RGdRM - North Side of RPdT

64716681159

14

Zonal Application Rate (AF/yr)

Zone Number

1

Appendix B page 16

Diagram of Mountain Front Recharge Distribution T17.0Averaolumnrow 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49

1 12 13 14 15 16 17 18 29 2

10 211 212 313 314 315 316 317 318 319 320 321 322 323 424 425 426 427 428 429 430 431 432 433 434 435 436 437 438 439 440 441 542 543 544 545 546 547 548 549 550 551 552 553 554 555 6 556 6 657 658 659 660 7 7 7 7 7 7 6

180450

Mountain Front Recharge Distribution

Zone Number

Zonal Recharge Rate (AF/yr)12601

234

7

56

270

63010801440

Appendix B page 17

Stress Period:

Taos Pueblo*

Town of Taos El Prado

Other Mutual

Domestic Wells

Domestic Well*

Multiple Dwelling Domestic

Wells*Sanitary Wells* Total

1964-1973 100 510 0 137 563 299 189 1608

1974-1983 200 680 0 183 563 299 189 1924

1984-1993 200 837 37 370 563 299 189 2305

1994-2003 200 838 64 395 563 299 189 2358

Well Pumping Input into Calibration Run of T17.0 Model (AF/yr)

* Estimated Diversions

Appendix B page 18

55

1010

1515

2020

3030

3535

4040

4545

5050

5555

6060

55 1010 1515 2020 2525 3030 3535 4040 4545 5050 5555 6060olumnsolumns

Row

sR

ows

11

Ranchos de Taos (2)Talpa (4)

2525

Canon (2)

Canon (1)

TalpaTalpa

Valdez

El Prado (3)

El Prado (2)

El Salto

Arroyo Seco

Llano Quemado (1)Llano Quemado (2)

Ranchos de Taos (1)

Upper Ranchitos

Upper Desmontes (1)Upper Desmontes (2)Lower DesmontesUpper Arroyo Hondo

Lower Arroyo Hondo

Rio Grande

Rio Hondo

Rio Fernando d

e Taos

Rio P

ueblo

deTaos

Arroyo

Alamo

LoboCreek

RioGrande del Rancho

Sou th Fork Rio Hondo

ArroyoHondo

Taos Mutual Domestic Wellsand El Prado WSD Wells

0 105Miles

Appendix B page 19

Municipal and Other Non-Domestic Water Supply Wells Simulated in Taos Groundwater ModelAveColumnRow4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49

12345 36 3 37 3 3 389

10 3 31112131415161718192021222324252627 4282930 431 132 133 134 1353637 23839 2 240 3 24142 243 24445 346 3474849505152535455 35657 3 358 359 3 360

Designation Wells

1 Taos Pueblo (estimated, generalized pumping location)2 Town of Taos3 El Prado Water & Sanitation District4 Mutual Domestic Associations

Appendix B page 20

Distribution of Domestic Wells and Sanitary Type Wells Simulated in Taos Groundwater Model Includes wells listed in OSE files as Domestic, Multiple (Domestic well serving multiple dwelling) and Sanitary

Numbers shown represents the number of these types of wells that occur in the model cells

SumColumnRow 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 32 33 34 35 36 37 38 39 40 41 42 43 44 45 46 47 48 49

1 1 1 1 5 12 1 2 1 1 13 2 2 4 1 1 1 3 2 1 1 14 1 1 6 3 4 2 2 1 1 4 2 35 1 1 1 4 5 4 1 1 1 1 1 2 2 1 3 3 4 2 1 7 1 66 3 2 2 3 2 5 2 4 5 3 1 3 1 4 4 5 6 2 1 1 1 17 3 1 2 4 2 1 1 1 1 3 1 1 3 1 1 6 5 4 4 6 4 5 5 4 6 1 38 1 1 2 2 2 3 1 1 1 2 1 1 3 8 5 2 2 1 3 2 2 2 4 11 49 2 1 1 2 2 2 2 2 1 6 3 1 1 1 4 9 10 4 8 3 4 2 1 3 5 8 3 3 3

10 1 4 1 2 3 1 1 1 2 1 1 1 1 3 8 1 6 12 6 4 1 3 1 6 4 3 1 411 1 1 1 2 4 2 1 1 1 1 2 1 1 1 2 3 6 6 212 4 3 1 1 1 113 1 1 1 1 1 2 2 1 1 3 5 114 1 2 1 1 2 2 1 1 3 3 115 1 1 1 2 116 2 1 1 1 1 1 4 7 117 1 1 4 2 1 1 118 1 1 1 1 2 219 1 1 1 1 1 2 220 1 2 1 1 1 121 1 1 1 1 1 4 122 1 1 2 1 1 1 7 3 8 1 123 1 1 1 1 2 1 1 1 7 9 6 2 224 1 1 1 1 1 5 2 4 3 1 125 1 1 2 1 2 4 1 4 6 2 1 126 1 1 1 3 4 4 4 4 1 827 1 1 1 2 2 1 1 1 4 4 1 2 7 328 2 1 1 1 4 4 2 3 4 4 2 129 1 1 1 4 1 4 3 3 1 4 130 2 1 4 2 8 1 2 3 2 231 1 1 1 3 2 1 1 1 332 1 1 1 1 2 2 3 2 2 4 233 4 3 4 3 2 1 3 5 134 3 2 1 2 1 1 4 2 135 4 5 7 1 1 1 4 3 236 1 1 1 3 2 5 3 2 1 1 1 137 2 1 1 1 6 9 1 1 2 3 1 1 138 1 6 2 4 10 4 5 1 139 2 3 5 1 5 8 3 2 1 1 140 3 2 1 1 1 341 1 1 2 2 1 1 2 1 2 342 1 1 1 1 5 5 3 1 2 3 143 1 1 1 3 5 7 5 1 2 1 2 3 4 3 144 1 3 3 8 2 3 9 3 1 1 4 5 1 1 5 1 3 145 1 5 1 3 1 5 2 4 3 3 1 4 4 946 2 2 3 3 1 3 4 2 1 1 2 3 2 7 5 247 1 2 1 7 3 3 2 2 1 2 1 3 2 3 3 2 4 448 1 2 2 2 3 2 3 1 3 3 1 2 2 2 1 1 3 4 5 1 549 1 1 3 2 2 2 3 1 2 1 3 6 2 2 1 1 1 2 3 2 150 1 1 3 2 5 1 2 1 4 2 1 1 1 1 1 1 3 2 1 2 3 151 3 2 4 3 2 7 1 2 5 2 5 4 2 2 5 3 3 352 1 2 2 1 1 1 4 5 2 3 4 6 2 9 5 7 3 3 4 1 5 3 153 1 2 1 1 2 4 6 2 3 1 5 6 4 9 8 5 3 3 5 5 7 3 454 1 1 1 1 1 4 1 5 2 1 1 2 7 6 5 4 3 1 4 4 8 5 5 255 1 3 4 9 4 5 6 2 1 4 13 3 5 4 2 3 5 1 6 2 5 156 1 1 2 1 1 1 1 1 6 11 6 4 4 5 8 1 4 2 8 1 5 4 3 4 257 1 1 1 1 1 1 1 1 3 4 4 3 1 2 3 4 3 1 558 2 1 1 1 2 1 2 3 4 2 6 8 2 159 2 1 1 1 1 2 5 10 3 260 1 1 1 2 1 4 4 5

Appendix B page 21

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Appendix C Detailed hydrogeologic background report:

Hydrologic Characteristics of Basin-fill Aquifers in the Southern San Luis Basin, New Mexico By Paul Drakos, Jay Lazarus, Bill White, Chris Banet, Meghan Hodgins, Jim

Riesterer and John Sandoval.

New Mexico Geological Society Guidebook, 55th Field Conference, Geology of

the Taos Region, 2004, p. 391-404.

Appendix C page 1

391New Mexico Geological Society Guidebook, 55th Field Conference, Geology of the Taos Region, 2004, p. 391-404.

INTRODUCTION

The Town of Taos, Taos Pueblo, and adjacent communities are situated primarily within the Rio Pueblo de Taos and Rio Hondo drainage basins. The Rio Pueblo de Taos basin includes the fol-lowing streams from north to south; Arroyo Seco, Rio Lucero, Rio Pueblo de Taos, Rio Fernando de Taos, and Rio Grande del Rancho (Figs. 1 and 3). Northern tributaries to Rio Pueblo de Taos drain Precambrian granite and gneiss, and Tertiary granite,

whereas southern tributaries drain Paleozoic sandstone, shale, and limestone (Kelson and Wells, 1989). The area of this study includes the region between the Sangre de Cristo mountain front on the east and the Rio Grande on the west, the Rio Hondo on the north and the Rio Grande-Rio Pueblo de Taos confluence on the south (Fig. 1).

The majority of the historic water supply for municipal, domes-tic, livestock, and sanitary purposes for the Town of Taos, Taos Pueblo, and adjacent communities has been derived from the

HYDROLOGIC CHARACTERISTICS OF BASIN-FILL AQUIFERS IN THE SOUTHERN SAN LUIS BASIN, NEW MEXICO

PAUL DRAKOS1, JAY LAZARUS1, BILL WHITE2, CHRIS BANET2, MEGHAN HODGINS1, JIM RIESTERER1, AND JOHN SANDOVAL2

1Glorieta Geoscience Inc. (GGI), PO Box 5727, Santa Fe, NM 875022US Bureau of Indian Affairs (BIA), Southwest Regional Office, 615 First St., Albuquerque, NM 87102

ABSTRACT.—The Town of Taos and Taos Pueblo conducted a joint deep drilling program to evaluate the productivity and water quality of the Tertiary basin-fill aquifer system underlying the Servilleta Formation. Testing results from a series of municipal, exploratory, subdivision, and domestic wells are also used to characterize hydrologic properties (T, K, K’, and S), and the effect of faults on groundwater flow in shallow and deep basin fill aquifers. The shallow unconfined to leaky-confined alluvial aquifer includes alluvial deposits and the underlying Servilleta Formation (Agua Azul aquifer facies). The deep leaky-confined to confined aquifer includes Tertiary age rift-fill sediments below the Servilleta Formation and is subdivided into the Chama-El Rito and Ojo Caliente aquifer facies. Although faults typically do not act as impermeable boundaries in the shallow alluvial aquifer and groundwater flow in the shallow aquifer is not significantly affected by faults, the Seco fault and several of the Los Cordovas faults act as impermeable boundaries in the deep basin fill aquifer. However, other Los Cordovas faults apparently do not affect groundwater flow in the deep aquifer, suggesting variable cementation along fault planes at depth. The Town Yard fault appears to be a zone of enhanced permeability in the shallow alluvial aquifer, and does not act as an impermeable boundary in the deep basin fill aquifer. Intrabasin faults such as the Seco fault that exhibit significant offset likely cause some compartmentalization of the deep aquifer system.

Colorado Plateau SL

E

A

S

P

M

Mogollon -Datil Volcanic

Field

Study AreaRio Hondo

RioPueblo de Taos

Rio

Gra

nde

State Rd. 68

State Rd. 68

US Hwy 64

Hwy. 150

US Hwy 64

Town of Taos

Sa

ng

re

de

C

ris

to

Mo

un

tain

sSymbol ExplanationMajor stream or river

1

1

0

0

1 Miles

1 Kilometers

Study Area Detail

G r e a t P l a i n s

Kilometers

Sout

hern

Roc

ky M

ount

ains

Jemez Lineament

Jemez Volcanic

Field

Rio

Gr a

nd

e

R

i ft

FIGURE 1. Location map – schematic map of New Mexico showing study area and the approximate limits of various physiographic provinces and geographic features. Major basins in the Rio Grande rift from north to south are: SL=San Luis, E = Española, A = Albuquerque, S = Socorro, P = Palo-mas, M = Mimbres. (state map modified from Sanford et al., 1995 and Keller and Cather, 1994).

Appendix C page 2

392 DRAKOS ET AL.

shallow stream-connected alluvial aquifer system. In an effort to minimize stream depletion effects resulting from new groundwa-ter development, the Town of Taos and Taos Pueblo, with funding from the U.S. Bureau of Reclamation (BOR), conducted a deep drilling program to evaluate the productivity and water quality of the Tertiary basin-fill aquifer system underlying the Servilleta Formation. The results of this drilling program, in conjunction with data collected from shallow basin fill and alluvial wells and additional deep exploratory wells, allow for a preliminary evalua-tion of aquifer characteristics, vertical connectivity of the shallow and deep aquifer systems, and the effect of faults on groundwater flow in the basin-fill aquifer system.

METHODOLOGY

A series of exploratory wells were drilled and tested during the deep drilling program and previous investigations to character-ize the basin fill aquifer system. Data from 45 pumping tests are used to determine aquifer characteristics and boundary effects, in particular to determine the effect (if any) of faults on groundwater flow. Well nests and nested piezometers were installed in several locations and pumping tests were configured to: 1) measure trans-missivity (T) and storage coefficient (S); 2) evaluate downward or upward leakage between aquifers induced by pumping stresses, and; 3) where possible, to calculate vertical hydraulic conductiv-ity (K’). Water-level data collected from wells in the different aquifers using electronic sounders, steel tapes, and transducers are used to construct potentiometric surface maps of the aquifers and are used to determine upward or downward vertical gradients at point locations.

STRATIGRAPHIC UNITS

From oldest to youngest, the units underlying the basin dis-cussed in this study are: 1) Pennsylvanian Alamitos Formation, 2) Tertiary Picuris Formation, 3) Tertiary Santa Fe Group, 4) Ter-tiary Servilleta Formation, and 5) Quaternary Alluvium. Galusha and Blick (1971) subdivided the Santa Fe Group into the Tesuque Formation and the overlying Chamita Formation. The Tesuque Formation is further subdivided into the Chama-El Rito Member and the overlying Ojo Caliente Sandstone Member (Fig. 2; Galu-sha and Blick, 1971). Although extending this Santa Fe Group stratigraphic nomenclature into the southern San Luis Basin may be problematic, it is used as an initial framework for this inves-tigation.

DESCRIPTION OF THE SHALLOW AQUIFER SYSTEM

Two major aquifer systems are identified in the Taos area: 1) A shallow aquifer that includes the Servilleta Formation and overlying alluvial deposits and, 2) A deeper aquifer associated with Tertiary age rift-fill sediments (Fig. 2). The lower Servilleta basalt and underlying Chamita Formation may act as a transition zone and/or boundary between the shallow and deep aquifers, although there are not currently enough data points in this inter-val to definitively support or refute this hypothesis.

The shallow aquifer system generally includes unconsolidated alluvial fan and axial-fluvial deposits overlying and interbedded with the Servilleta basalt flows. The shallow aquifer is subdi-vided on the basis of lithology and pumping test analyses into: 1) unconfined alluvium; 2) leaky-confined alluvium, and; 3) the Servilleta Formation (Fig. 2). Several wells in the study area are completed into shallow aquifers in fractured Paleozoic sedimen-tary formations and fractured Precambrian crystalline rocks along the Sangre de Cristo mountain front. These aquifers discharge to alluvium and/or the Servilleta Formation and are therefore part of the shallow alluvial-aquifer flow system. The shallow alluvial aquifer has a maximum thickness of 1500 ft (457 m) or more in the graben formed by the down-to-the-west Town Yard fault and the down-to-the-east Seco fault (Drakos et al., this volume), and pinches out in the western part of the study area where the allu-vium is unsaturated at the Taos Airport domestic well (Fig. 4).

Hydrologic Characteristics of the Shallow Aquifer

Aquifer testing data are available for the shallow aquifer from 32 pumping tests at locations throughout the study area (Fig. 4; Table 1). Pumping tests were run for times ranging from 350 to 12,960 minutes (min) at discharge (Q) ranging from 18 to 440 gallons per minute (gpm) (Table 1).

Aquifer Stratigraphic Unit

UnconfinedQal

Leaky-confined Qal(Includes Lama Fm.)

transition

Dee

p Te

rtiar

y B

asin

Fill

(leak

y-co

nfin

ed &

con

fined

)

BasinMarginLower Serv. Basalt

Chamita Fm. (FracturedPaleozoic

sedimentary,metasedimentary,

andcrystalline

rocks)

Middle Serv. Basalt

Upper Serv. BasaltAgua Azul

Ojo Caliente Mbr.

Chama-ElRito Mbr.

Picuris Fm.

Tesu

que

Fm.

Shallow(unconfined-

leakyconfined)

Ser

ville

ta F

m.

W E

FIGURE 2. Taos Valley geohydrologic framework

Appendix C page 3

393HYDROLOGIC CHARACTERISTICS OF BASIN-FILL AQUIFERS

68

150522

64

64

Map grid, NAD 1927, UTM Zone 13, meters

Rio Hondo

Rio

Luce

ro

RioPueblo de Taos

Rio Fernando de Taos

Rio

Grande

del Ranch o

RioPue

blo de Taos

Rio

Gra

nde

Arro

yoS

eco

Los Cordovas Fault Zone

?

?

?

?

?

?

?

??

?

?

?

Gorge ArchSeco

Fault Tow

nYa

rdFa

ult

Tow

nYa

rdFa

ult

Sang

rede

Cris

toFa

ult Z

one

?

Gorge

Fault

Leaky-confined Alluvial WellAgua Azul Well

Unconfined Alluvial WellSymbol Explanation

Fault, inferred from surfaceor drilling data, ball and baron downthrown sideAnticline

Syncline

Major stream or riverMajor road

Kilometers

Ojo Caliente + Chamita WellChama-El Rito Well

3 San

gre d

e Cristo

Mtn

s.

Mariposa Ranch

Cielo Azul Deep

Bear Stew

BIA 17BIA 24

McCarthyBIA 9

BOR 5

BIA 20Quail Ridge

BIA 2

BIA 14

BIA 1

Howell

TOT#3

Kit Carson

TOT#5

BOR2A

TOT #26.9

La Percha

Cooper

Arroyo Park 18.8

BIA 15

BIA 11

Colonias Point

Taos SJC

Ranchos Elem. School

Ruckendorfer

BJV#1

Riverbend

Arroyos del Norte

Cameron

BIA 7

BOR 7

TOT Airport

BOR 6

K3

Town YardBOR 2B BOR 3

RP2500

BOR1 UNM/Taos

National Guard

FIGURE 3. Map of study area with pumping test well locations

Appendix C page 4

394 DRAKOS ET AL.

Confined QalLow K zone

Confined QalHigh K Zone

Rio Hondo

Rio

Luce

ro

RioPueblo de Taos

Rio Fernando de Taos

Rio

Grande

del Ranch o

RioPue

blo de Taos

Rio

Gra

nde

Arro

yoS

eco

ueblo d

uebbloo d

Unsa

tura

ted

Allu

vium

Los Cordovas Fault Zone

?

?

?

?

?

?

?

??

?

?

?

Gorge ArchSeco

Fault Tow

nYa

rdFa

ult

Tow

nYa

rdFa

ult

Sang

rede

Cris

toFa

ult Z

one

?

Gorge

Fault

Leaky-confined Alluvial WellAgua Azul Well

Unconfined Alluvial Well

BIA 91.9

- Well name - Hydraulic Conductivity (ft/day)

Symbol Explanation

Fault, inferred from surfaceor drilling data, ball and baron downthrown sideAnticline

Syncline

Major stream or river4040000 Map grid, NAD 1927, UTM Zone 13,

meters

Kilometers

TOT Airport Dom.Qal Dry

Mariposa Ranch2.9 Cielo Azul Deep

0.4

Bear Stew3.3

BIA 170.6

BIA 240.1

McCarthy3.6

BIA 91.9

BOR 50.3

BIA 200.2

Quail Ridge4.0

BIA 217.4

BIA 143.7

BIA 14.3

Howell12.5

TOT#36.4

Kit Carson7.0

TOT#516.0

BOR2A29

TOT #26.9

La Percha3.0

Cooper4.7

Arroyo Park 18.8

BIA 151.6

BIA 110.9

Colonias Point17.1

Taos SJC8.6

Ruckendorfer0.1BJV#1

22.0

Riverbend26.7

Arroyos del Norte11.0

Cameron2.1

FIGURE 4. Map of shallow aquifer wells with K values from pumping tests

Appendix C page 5

395HYDROLOGIC CHARACTERISTICS OF BASIN-FILL AQUIFERS

Unconfined alluvium

Pumping tests on 18 unconfined alluvial wells exhibit hydrau-lic conductivity (K) values ranging from 1.8 to 22 ft/day (mean = 6.8 ft/day, ± (1σ) 5.9 ft/day). No clear pattern is observed in geographic distribution of K in the unconfined alluvial aquifer (Fig. 4). The K value calculated at a given location is likely con-trolled by local facies changes (e.g. better sorted axial fluvial deposits yield higher K values than less well sorted overbank or fan deposits) and well design (e.g. whether the well was drilled and screened to sufficient depth to encounter a productive zone). Pumping tests were not run long enough to observe delayed yield and allow for a calculation of specific yield (Sy), but storativity (S) ranged from 10-4 to 10-2. Possible recharge boundaries were observed in the TOT#3 and TOT#1 tests, and, although data are somewhat ambiguous, an impermeable boundary may be indi-cated in the BJV#1 test (Table 1). The possible recharge bound-ary observed in the TOT#3 and TOT#1 tests is likely a result of leakage into the shallow aquifer from the nearby Rio Pueblo de Taos and Rio Lucero.

Leaky-confined alluvium

Pumping tests on nine leaky-confined alluvial wells exhibit K values ranging from 0.1 to 17.4 ft/day, and fall into two distinct populations and geographic groupings. Low-K (mean K = 0.4 ft/day) northern wells correspond to older Blueberry Hill mudflow or weathered fan deposits underlying the large Rio Hondo allu-

vial fan at the northern portion of the study area. High-K (mean K = 11.4 ft/day) values observed in southern wells correspond to young (?), less-weathered deposits underlying the small Rio Pueblo de Taos fan (Fig. 4). The Howell well and BIA 2 (Buf-falo Pasture) wells, which both exhibit high K values of 12 to 17 ft/day, lie along the northern trace (approximately located) of the Town Yard fault (Fig. 4). This segment of the fault may be a high-permeability zone or may be coincident with high-perme-ability Rio Lucero and/or ancestral Rio Hondo or Rio Pueblo de Taos channel fill deposits. The Town Yard fault may have been a control on stream channel location during aggradation of paleo-Rio Pueblo de Taos or paleo-Rio Hondo deposits. The Town Yard fault projects into the present day Rio Lucero drainage, and the “Seco fault” projects into the Arroyo Seco drainage (Fig. 4).

Servilleta Formation (Agua Azul aquifer)

Aquifer testing data are available for the Servilleta Forma-tion from five pumping tests (Fig. 4, Table 2). All wells tested are completed into the “Agua Azul” aquifer between the upper and middle basalt flow members and are located along the Rio Pueblo de Taos and Arroyo Seco drainages (Fig. 4). Pumping test duration ranged from 2,880 to 5,760 min at Q ranging from 8 to 120 gpm (Table 2). Agua Azul wells exhibit K ranging from 4.7 to 26.7 ft/day (mean K = 12.0 ± 8.6 ft/day). Because the five wells tested in the “Agua Azul” aquifer are relatively close to one another (Fig. 4), determining the geographic distribution of K is not possible. Storativity values range around 10-4.

Well NameTD(ft)

StaticDTW (ft)

Testlength(min) Q (gpm) T (ft2/day) b (ft) K (ft/day)

Storagecoefficient

Boundariesobserved Source Comments

Unconfined alluviumColonias Point 127 55 2880 36 1,200 70 17.1 n.a. none GGI well pumped at maximum Q of existing pumpQuail Ridge 150 45 2880 22 400 100 4.0 1.2 x 10-2 none GGI calculations from obs. well data, r = 35 ftTOT #1 182 43 400 125 830 140 5.9 5.2 x 10-4 none/ GGI calculations from obs. well data, r = 50 ftMcCarthy 193 84 2880 18 400 110 3.6 n.a. none GGITOT #2 204 42 355 205 760 110 6.9 8.6 x 10-4 none GGI calculations from obs. well data, r = 50 ftBIA 15 225 116 1600 41 150 95 1.6 2.5 x 10-2 none BIA observation well data, r = 21 ftBJV#1 240 158 5760 68 1,980 90 22.0 1.0 x 10-3 none/ imperm? GGI Theis curve is very poor fit; obs well data suggest impermeable

boundaryKit Carson 270 64 480 100 1,400 200 7.0 n.a. none GGIBOR 2A 291 61 250 45 230 80 2.9 n.a. none GGITOT #3 312 60 350 180 960 150 6.4 n.a. none/ GGI T calculated from obs. well data, r = 18 ftTOT#5 330 14 1720 370 3,700 230 16.1 n.a. none GGIBear Stew 339 46 1300 33 968 290 3.3 n.a. recharge? BIACameron 350 107 2880 50 500 240 2.1 n.a. none GGILa Percha 360 105 2880 69 700 235 3.0 n.a. none GGIBIA 1 400 92 1440 180 825 190 4.3 n.a. none BIA T = avg of Pump & Rec semilog plotsBIA 9 575 470 1400 18.5 230 120 1.9 3.0 x 10-4 none BIA T calculated from obs. well data, r = 23.1 ftMariposa Ranch 781 585 2880 31-49 580 200 2.9 n.a. none GGI well dev. during pumping; T from rec dataArroyos del Norte 800 659 2880 55 1,100 100 11.0 n.a. none GGI

Confined or leaky-confined alluviumSouthern wellsHowell 500 13 12960 440 5,000 400 12.5 6.3 x 10-3 leaky/recharge GGI T and S calculated from obs. well data, r = 485 ft; k' = 0.2 ft/dayBIA 14 613 -1 2800 70 810 220 3.7 n.a. none BIABIA 2 700 18 1440 300 5,700 440 17.4 6 x 10-3 leaky/recharge BIA S calculated from obs. well data, r = 47 ft

Northern wellsBIA 17 470 86 1440 19 230 385 0.6 n.a. leaky/recharge BIABIA 11 760 100 2800 70 310 330 0.9 1 x 10-3 none BIA S calculated from obs. well data (30'screen), r = 147 ft;Cielo Azul deep 850 339 2880 20 40 100 0.4 n.a. none BIA no drawdown observed in adjacent shallow well during testBIA 24/ Grumpy 1000 177 944 25 32 400 0.1 n.a. none BIA Blueberry Hill Fm?BIA 20/ West 1018 111 1120 50 120 600 0.2 n.a. none BIA Blueberry Hill Fm?BOR 5 1763 265 5760 40 110 400 0.3 n.a. none BIA Blueberry Hill Fm?

TABLE 1. Aquifer testing data from unconfined and confined/leaky confined alluvial wells, southern San Luis basin. DTW = depth to water; Q = discharge; T = transmissivity; b = aquifer thickness; K = hydraulic conductivity. Well locations included in Appendix A.

Appendix C page 6

396 DRAKOS ET AL.

Groundwater Flow Direction in the Shallow Aquifer System

A composite alluvial and Agua Azul (Servilleta) potentiomet-ric surface map representing the shallow alluvial aquifer was con-structed from water levels measured to the nearest 0.01 ft from wells that could be assigned to a specific aquifer. In the northeast part of the study area, a downward vertical gradient was observed in the alluvial aquifer, with up to 200+ ft (60+ m) head differ-ence in adjacent wells (e.g. well nests Cielo Azul shallow and deep, BIA20/BOR5, Mariposa shallow/deep; Fig. 5). Where strong downward vertical gradients are observed, the shallower water level was used for construction of the potentiometric sur-face map. Water levels from Agua Azul wells were included with the alluvial well data, because the Agua Azul aquifer interfingers with the alluvium near the mountain front and in the southern part of the study area, and water levels in the Agua Azul are similar to those measured in the unconfined alluvium.

In addition to groundwater elevations measured in wells throughout the study area, streambed elevation data are incor-porated into the construction of the potentiometric surface map. Streambed elevations were determined from USGS 7.5’ quad-rangles and added as elevation control points to the base map. Equipotential lines are contoured so that groundwater elevation is less than or approximately equal to streambed elevation. Equipo-tential lines lie consistently lower than streambed elevation along the lower Rio Pueblo de Taos and the Arroyo Seco, indicating a disconnection between surface water and groundwater in those areas.

Groundwater flow direction in the composite Alluvial plus Aqua Azul (Servilleta) aquifer system is from northeast to south-west and east to west (Fig. 5). A broad groundwater trough is observed north of Rio Pueblo de Taos and west of Rio Lucero (Fig. 5). At its northern end the trough axis projects into the Rio Hondo drainage (Fig. 5), and the trough lies along the eastern side of the large Rio Hondo fan north of Rio Pueblo de Taos. This trough may correspond to an area of high-permeability fluvial deposits associated with the ancestral Rio Hondo, and is coinci-dent with a structural low (Lipman, 1978, p. 42) or Rio Pueblo de Taos syncline of Machette and Personius (1984) and Dungan et al. (1984), suggesting a structural control on the location of the ancestral Rio Hondo drainage. However, the location of the river has been restricted to near its present course since stream incision occurred in response to rapid cutting of the Rio Grande gorge ca. 0.6 to 0.3 Ma ago (Wells et al.,1987; Kelson and Wells, 1987). Since that time, the Rio Hondo has been an entrenched

stream flowing very close to its present location (Kelson and Wells, 1987, Kelson and Wells, 1989). Other high transmissivity zones associated with axial stream deposits have been identified along the Rio Grande del Rancho (within the Miranda graben) and along the Rio Fernando (Spiegel and Couse, 1969; Bauer et al., 1999). A groundwater high is observed in the vicinity of the lower Arroyo Seco drainage on the west side of the Town of Taos, corresponding to the area between the Gorge arch and the Rio Pueblo de Taos syncline (Fig. 5). The composite Alluvial plus Servilleta aquifer system becomes unsaturated in the western part of the study area, indicating this upper aquifer is discharging to surface water where it is stream connected and/or leaking into the deeper basin-fill aquifer. The steepening gradient in the vicinity of the Los Cordovas faults suggests that the faults are an area of downward leakage through which the shallow aquifer may be recharging the deep aquifer system.

Equipotential lines are deflected downstream along most of the Arroyo Seco and the upper Rio Lucero, indicating that these are losing streams west of the mountain front (Fig. 5). Based on equipotential lines, the upper Rio Hondo is a gaining reach, whereas the lower Rio Hondo is a losing reach. Equipotential lines are generally deflected upstream along the Rio Pueblo de Taos, lower Rio Lucero, and Rio Fernando de Taos, indicating that these streams are gaining reaches (Fig. 5).

In January and June 2000, personnel from the BIA, GGI, and the BOR measured flows in Taos valley rivers (Rio Hondo, Arroyo Seco, Rio Lucero, Rio Fernando de Taos, Rio Pueblo de Taos, Rio Grande del Rancho). Flows were measured in January and June to determine seasonal variations in stream loss or gain. Acequia diversions from and return flows to each river were also measured and accounted for in the flow data to allow for a determination of gaining or losing reaches (see Smith, 2001 and 2002, unpubl. BOR reports, for results of this study). Figure 5 summarizes the results of the January, 2001 stream gaging, showing losing, gain-ing, and no net change reaches of the major stream systems. In general, results of stream gaging correlate well with gaining and losing reaches derived from construction of the potentiometric surface map described above. However, two significant differ-ences are observed between the gaging data and the potentiomet-ric surface map: 1) gaging data show the upper reaches of the Rio Hondo as losing reaches, while the equipotential lines suggest it is a gaining reach, and 2) gaging data indicate the upper reach of the Rio Lucero is gaining, while the potentiometric surface map suggests it is a losing reach (Fig. 5). These differences may be a result of the groundwater elevation representing long-term

Well Name TD (ft) StaticDTW (ft)

Testlength(min)

Q (gpm) T (ft2/day) b (ft) K (ft/day) Storagecoefficient

Boundariesobserved Source Comments

Cooper 180 96 2880 31 280 60 4.7 n.a. none GGIArroyo Park 262 105 2880 48 530 60 8.8 5.3 x 10-4 none GGI S calc from obs well, r = 2000 ftTaos SJC 180 29 5760 120 430 50 8.6 2.5 x 10-4 none GGI calculations from observatin well data,

r = 25 ft;k' = 0.02 ft/dayBarranca del Pueblo 233 2880 7.5-12 670 60 11.2 n.a. none RE/SPEC b is unknown; 60 ft used as default aquifer

thicknessRiverbend 215 121 2880 54 1,600 60 26.7 8.5 x 10-5 none GGI

TABLE 2. Aquifer testing data from Servilleta Formation sediments and fractured basalt (Agua Azul) wells, southern San Luis Basin. Well locations included in Appendix A.

Appendix C page 7

397HYDROLOGIC CHARACTERISTICS OF BASIN-FILL AQUIFERS

FIGURE 5. Shallow aquifer potentiometric surface map, gaining and losing stream reaches

Map grid, NAD 1927, UTM Zone 13, meters

Rio Hondo

Rio Lucero

RioPueblo de Taos

Rio Fernando de Taos

Rio

Grande

del Ranch o

RioPue

blo de Taos

Rio

Gra

nde

Arroyo Seco

ueblo d

uebbloo d

DownwardVertical Gradient

Unsa

tura

ted

Allu

vium

Los Cordovas Fault Zone

?

?

?

?

?

?

?

??

?

?

?

Gorge Arch

SecoFault Tow

nYa

rdFa

ult

Tow

nYa

rdFa

ult

Sang

rede

Cris

toFa

ult Z

one

?

Gor

geFa

ult

Explanation

Fault, inferred from surface or drilling data, ball and bar on downthrown side

Anticline Syncline

6600 Groundwater elevation contour, contourn interval = 100 ft

Kilometers

Stream Gaging StationGaining Reach*Losing Reach*No net gain or loss*

No gage data*Net gain or loss determined from stream gaging conducted by GGI, BOR, & BIA in January, 2000.

Dry reach

Leaky-confined Alluvial WellAgua Azul Well

Unconfined Alluvial Well

BIA 2700

7074

- Well name - Total depth (ft)- GW Elevation (ft)

Basin Margin Well

7400

73007200

7100

7000

69006800

7100

7200

7300

7400

7000

69006800

670066

00

6500

6700

6600

6500

7500

7500

7600

7600

7700

?

?

??

TOT Airport Dom.Qal Dry

Dickerson425

7014Mariposa Ranch

295/8007148/6826

Adelman290

7351

Porter220

7420

Yaravitz400

7746

Cielo Azul Shallow3537305

Cielo Azul Deep8507103

Bear Stew339

7474

BIA 17470

7423

BIA 2410007226

McCarthy193

7286

BIA 95756847

BOR 517636983

BIA 2010187137

Quail Ridge1507170

Cameron350

7051

BIA 2700

7074

BIA 14613

7004

BIA 1400

6971

Howell500

6948TOT#3

3126930

Kit Carson270

6926TOT#5

3306939

BOR2A291

6813

TOT 1&2182/204

6926/6937

Fred Baca Park75

6869

La Percha360

6862

Amos' Well122

6687

Cooper1806793

Arroyo Park 1262

6804

BIA 15225

6650

Landfill MW12947069

BIA 117607100

Colonias Point1277100

Taos SJC180

6630Gardiner

1356789

Ranchos Elem. School140?6919

Ruckendorfer6006899

BJV#12406733

Riverbend2156611

Baranca del Pueblo3206454

Arroyo Seco Plaza740

7560

K2 Screen 7

2066905

Arroyos del Norte800

6828

Old Ranch?

7115

Hail Ck.25/180

6959/6945

Appendix C page 8

398 DRAKOS ET AL.

conditions, while the gaging data are a snapshot of conditions at a particular time. It is also possible that some surface diversions from, or additions to, the rivers may not have been accounted for or may have been variable during the gaging study.

Effect of Faults on the Shallow Aquifer

Unconfined and leaky-confined alluvium

Twenty-seven pumping tests have been conducted on alluvial wells, nine of which were conducted on wells completed into the leaky-confined alluvial aquifer facies, and five of which were additional tests conducted on Agua Azul (Servilleta) wells. Of these tests, data from only one well near the southern portion of the study area (BJV#1) suggest impermeable boundary effects (Table 1). Pumping test data from numerous other wells located in close proximity (< approximately 0.5 mi or 0.8 km) to faults do not show impermeable boundary effects (Fig. 4; Table 1). As examples, the Howell, BIA2, and possibly Bear Stew wells are located along the Town Yard Fault; Quail Ridge, Cameron, and TOT#5 are located along the Seco fault; and BIA 15 is located near one of the Los Cordovas faults. Data from the BJV#1 test is suggestive of an impermeable boundary, which may correspond to a southern extension of the western Los Cordovas fault (Fig. 3). The down-to-the-west Los Cordovas fault would likely juxta-pose a thick clay against the underlying relatively thin water-pro-ducing sandy gravel described in the BJV#1 well log (Lazarus, unpubl. GGI report for BJV properties, 1989). In contrast, data from three wells located along the northern segment of the Town Yard fault (Howell, BIA 2, and Bear Stew wells) indicate leak-age or recharge boundaries, suggesting that the northern segment of the Town Yard fault may be a zone of enhanced permeability. Alternatively, as discussed above, the northern Town Yard fault may be coincident with an area of deposition of high-permeabil-ity axial channel deposits.

Based on the well density used to construct the potentiometric surface map and the 100-ft contour interval utilized, equipotential lines in the unconfined and leaky-confined alluvial aquifers are not strongly affected by the major faults in the basin (Fig. 5). This is consistent with the aquifer testing data, which indicate that, except in rare cases, intrabasin faults do not act as barri-ers to groundwater flow in the shallow alluvial aquifer. In some cases, such as the northern segment of the Town Yard fault, intra-basin faults may act as zones of enhanced permeability in the alluvium.

Servilleta Formation (Agua Azul aquifer facies)

Neither recharge nor impermeable boundaries were observed in any of the five tests for which data are available (Table 2). This is an unexpected result, given the relatively thin producing inter-val (50-60 ft thick [15-20 m]) aquifer and the proximity of Agua Azul wells to several of the Los Cordovas faults, in particular the proximity of the Taos SJC well to the western Los Cordovas fault strand (Fig. 4).

Aquifer Anisotropy/Vertical Hydraulic Conductivity

Alluvium

Data on vertical hydraulic conductivity (K’) and aquifer anisotropy are available from one location in the shallow aqui-fer system. The Howell well pumping test configuration included observation wells completed in both the deep leaky-confined and shallow stream-connected unconfined alluvial aquifers (Hail Creek shallow/deep; Fig. 5). Based on the Hantush-Jacob (1955) leaky-confined aquifer solution, a K’ of 0.2 ft/day was calculated. Based on the Howell well pumping test, horizontal K is approxi-mately 60 times vertical K.

Servilleta Formation (Agua Azul)

Data on K’ and aquifer anisotropy are available from one loca-tion in the Servilleta Formation. The Taos SJC well pumping test configuration included observation wells completed in both the Agua Azul and the overlying shallow stream-connected uncon-fined alluvial aquifer (GGI, unpubl. consulting report to the Town of Taos, 1997). Based on the Hantush-Jacob (1955) leaky-con-fined aquifer solution, a K’ of 0.02 ft/day through the USB was calculated. Horizontal K is approximately 430 times vertical K at that location.

DEEP TERTIARY BASIN FILL AQUIFER

The deep Tertiary basin fill aquifer includes generally weakly to moderately cemented eolian, alluvial fan, fluvial, and volcani-clastic deposits that underlie the Servilleta Formation. The deep Tertiary basin fill aquifer includes the Chamita Formation, the Ojo Caliente Sandstone Member of Tesuque Formation, the Chama-El Rito Member of Tesuque Formation, and the Lower Picuris Formation (Fig. 2). Pumping test data are available for the Ojo Caliente Sandstone Member of Tesuque Formation, the Chama-El Rito Member of Tesuque Formation, but are not available from wells completed solely in the Chamita or Picuris Formation.

The Tertiary basin fill aquifer exhibits confined or leaky-con-fined characteristics in the central and eastern part of the study area, but is likely unconfined in the western part of the study area along the Rio Grande. A deep fractured crystalline rock aquifer at or near the Sangre de Cristo mountain front may discharge to the deep basin fill aquifer system, but no wells are known to be completed into this zone. The Chamita Formation and the over-lying Servilleta Formation, while not extensively studied, may represent a transition zone between the shallow and deep aqui-fer systems (Fig. 2). The deep aquifer is, where investigated thus far, greater than 2000 ft thick. However, the Taos graben, within which the study area lies, has a depth of approximately 5 km (16,000 ft) (Cordell, 1978; Bauer and Kelson, this volume), so further investigations may show the deep aquifer to be signifi-cantly thicker than is presently known.

Appendix C page 9

399HYDROLOGIC CHARACTERISTICS OF BASIN-FILL AQUIFERS

Hydrologic Characteristics of the Deep Aquifer

Ojo Caliente Sandstone Member of Tesuque Formation

Aquifer testing data are available from five wells completed entirely or predominantly in the Ojo Caliente Sandstone Member of the Tesuque Formation (Fig. 6). Three of the tests were mul-tiple-well pumping tests (Table 3). Wells completed into the Ojo Caliente range in depth from 1720 to 2991 ft (524 to 912 m; Table 3), and exhibit pressure head (height of water column above the screened interval in a well) ranging from 500 ft (150 m) in the Airport well to greater than 1700 ft (500 m) in BOR7. Pumping test durations ranged from 1,361 to 11,965 min at Q ranging from 57 to 400 gpm (Table 3). Ojo Caliente wells exhibit K ranging from 0.2 to 0.8 ft/day (mean K = 0.4 ± 0.25 ft/day). Hydraulic conductivity in the Ojo Caliente is relatively consistent through-out the area and does not show variability relative to geographic location (Fig. 6). S values range from 1 x 10-3 to 2 x 10-2 (Table 3).

Chama-El Rito Member of Tesuque Formation

Aquifer testing data are available from five wells completed entirely or predominantly into the Chama-El Rito Member of the Tesuque Formation, three of which are multiple-well tests (Fig. 6; Table 4). Wells completed into the Chama-El Rito Member range from 1200 ft (365 m) to 2109 ft (643 m) in depth (Table 4), and exhibit pressure head ranging from 590 ft (180 m) at UNM/Taos to greater than 1300 ft (400 m) (BOR3). Pumping tests were run for times ranging from 2,737 to 15,840 min at Q ranging from 60 to 500 gpm (Table 4). Chama-El Rito wells exhibit K ranging from 0.6 to 3.4 ft/day (mean K = 1.8 ± 1.0 ft/day). Aquifer testing data for the Chama-El Rito Member are only available for the southern part of the study area so the geographic distribution of K throughout the basin is unknown. An S of 5 x 10-4 was calculated from the BOR3/BOR2 pumping test. All Chama-El Rito wells exhibited a confined or leaky-confined response during pump-ing tests. These data, in conjunction with the large pressure head observed in Chama-El Rito wells, indicates that the portion of the Chama-El Rito Member investigated thus far is a confined or leaky-confined aquifer.

Groundwater Flow Direction in the Deep Tertiary Aquifer System

Water level data from deep wells in the basin were used to construct a preliminary potentiometric surface map of the deep basin fill aquifer. These limited data suggest that groundwater flow direction in the deep aquifer is generally from east to west, at a relatively shallow gradient of approximately 0.004 ft/ft (Fig. 6). The shallow alluvial aquifer system has a much steeper gradi-ent (measured north of and parallel to the Rio Pueblo de Taos) of approximately 0.02 ft/ft. Although the head in the shallow aquifer system is much higher in the eastern part of the study area along the Sangre de Cristo mountain front, the potentiometric surfaces in the shallow and deep aquifers project toward one another in the western part of the study area. Head in the shallow alluvial aquifer is approximately from 100 to 200 ft higher than the head in the deep aquifer just east of where the shallow aquifer becomes unsaturated, suggesting the shallow aquifer discharges to the deep aquifer system in this general area.

Vertical gradients in the deep aquifer are observed at several well nests in the study area. Downward gradients are observed in the deep basin fill aquifer at well nests BOR4/BOR6, BOR7/BIA9, BOR1/NGDOM, and BOR2/BOR3, whereas upward gra-dients are observed at RP2500/RP2000 and K2/K3. Both well nests with upward gradients (BOR2/BOR3 and K2/K3) are located along the approximate trace of the Rio Pueblo de Taos syncline (Fig. 6; Lipman, 1978). These data suggest recharge to the deep aquifer at or near the basin margin migrates downdip within the syncline resulting in an upward pressure head along the fold axis.

Effect of Faults on Groundwater Flow

Ojo Caliente Sandstone Member of Tesuque Formation

Impermeable boundary effects were observed in K2/K3, RP 2500/RP2000, and BOR6/BOR4 pumping tests (Table 3). K3/K2 and BOR6/BOR4 are located within approximately 0.5 mi (0.8 km) of the Seco Fault (Fig. 6). The Servilleta Formation is offset approximately 950 ft across the down-to-the-east Seco fault (Drakos et al, 2001). The Seco fault is interpreted as the

Well Name TD (ft) StaticDTW (ft)

Testlength(min)

Q (gpm) T (ft2/day) b (ft) K (ft/day) Storagecoefficient

Boundariesobserved Source Comments

K3 - K2 1796 271 10,000 400 200 (early) 90 (late)

960 0.2 1 x 10-3 to2 x 10-2

impermeable BIA calculations from obs well, r = 65 ft; no drawdown observed in overlying aquifer

RP2500/RP2000

2500 152 11,965 400 250 (early) 60 (late)

1,200 0.2 1.4 x 10-3 impermeable GGI calculations from obs well, r = 95 ft; no drawdown observed in overlying aquifer

Airport 1720 500 2,760 57 250 685 0.4 n.a. none GGI well developed during test; T is suspectBOR6/BOR4

2020 610 10,059 365 640 810 0.8 7 x 10-3 impermeable BIA T and S calc from BOR4 late obs well late time data; r = 103 ft

BOR7 2991 732 1,361 70 110 480 0.2 n.a. none BIA

TABLE 3. Aquifer testing data from wells completed in Ojo Caliente Sandstone Member of Tesuque Formation, southern San Luis Basin. Well locations included in Appendix A.

Appendix C page 10

400 DRAKOS ET AL.

Los Cordovas Fault Zone

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Gorge ArchSeco

Fault

Tow

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rdFa

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Tow

nYa

rdFa

ult

Sang

rede

Cris

toFa

ult Z

one

?

Gorge

Fault

Rio Hondo

Arroyo Seco

Rio

Luce

ro

RioPue

blode Taos

Rio Fernando de Taos

Rio

Grande

del Ran cho

RioPue

blo de Taos

Rio

Gra

nde

Chama-El Rito WellOjo Caliente + Chamita Well

Basin Margin Well

BOR 6 (0.8)20206592

Impermeable

- Well name (k, ft/day)- Total depth (ft)- GW Elevation (ft)- Boundary type (if any)

Symbol Explanation

Fault, inferred from surfaceor drilling data, ball and baron downthrown sideAnticlineSynclineMajor stream or river

Kilometers

Map grid, NAD 1927, UTM Zone 13, meters

Groundwater elevationcontour, interval = 100 ft

6600

6600

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6700

6700

6600

6500

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BIA 7 (ND)10206597

BOR 7 (0.2)29916585

TOT Airport (0.4)17206564

BOR 6 (0.8)20206592

Impermeable

K3 (0.1-0.2)17966669

Impermeable

Town Yard (1.3)10206809

BOR 2B (0.6)14806788

BOR 3 (0.9-1.3)21096601

RP2500 (0.05-0.2)25006500

Impermeable

BOR1 (1.0-2.8)20036651

Impermeable

UNM/Taos (3.4)12006674

National Guard (3.4)14006663

Impermeable

FIGURE 6. Potentiometric surface map and K values for deep basin-fill aquifer

Appendix C page 11

401

impermeable boundary observed in the K3 and BOR6 pumping tests. RP2500 is located between two of the Los Cordovas faults; one or both of which likely act as impermeable boundaries. As discussed above, similar impermeable boundary effects were not observed in the 180-ft deep Taos SJC well, located adjacent to RP2500. These data suggest that either 1) the Los Cordovas fault(s) near RP2500 exhibit much greater offset with depth, or 2) that impermeable boundary effects are offset by leakage into the shallow aquifer, but are not offset by leakage at depth. The Ojo Caliente has an apparent thickness of > 1200 ft (370 m) at RP2500 (Drakos and Hodgins, unpubl. GGI report for the Town of Taos, 2001), so either the fault plane is a very low-permeability zone, or offset at depth is significant.

Impermeable boundary effects were not observed in the Air-port well and BOR7 pumping tests. Both tests were run for much shorter duration (less than 3000 min) at lower discharge than were the three Ojo Caliente tests discussed above (10,000 min or more; Table 3). The BOR7 test was likely not run long enough to observe the Seco fault as a possible boundary; however, from the very close proximity of the Airport well to the western Los Cor-dovas fault (Fig. 6) it is likely that the cone of depression would have intersected the fault plane during the pumping test. One pos-sible explanation for the absence of an impermeable boundary is that offset on the western Los Cordovas fault is dying out to the north, and Ojo Caliente sediments are juxtaposed against one another across the fault.

Chama-El Rito Member of Tesuque Formation

Impermeable boundary effects were observed in one pump-ing test conducted in the Chama-El Rito Member of the Tesuque Formation (BOR1/NGDOM pumping tests; Table 4). The imper-meable boundary observed in the BOR1/NGDOM pumping tests is likely the southern extension of one of the Los Cordovas faults. The possibility that the Los Cordovas faults extend south of the Rio Pueblo de Taos is suggested by Bauer and Kelson (this volume). Impermeable boundary effects are not observed in the UNM/Taos pumping test, suggesting that the imperme-able boundary observed in the BOR1/NGDOM pumping tests are related to faults in the eastern rather than the western portion of the Los Cordovas fault zone (Fig. 6). The southern extension of

the trace of the eastern Los Cordovas fault shown in Figures 4-6 is coincident with a fault interpreted from geophysical data from Reynolds (unpubl. consulting report to BIA, 1989).

A series of pumping tests were conducted on the BOR2/BOR3 well nest, located in relatively close proximity to the Town Yard fault (Fig. 6). Test data from BOR2B and BOR2C indicate that the Town Yard fault does not act as an impermeable boundary at this location. Test data from BOR3 were indicative of a weak nega-tive boundary, suggesting a facies change from coarser-grained to finer-grained deposits at some distance from the well (Drakos, Hodgins, Lazarus, and Riesterer, unpubl. GGI report for the Town of Taos, 2002). The Town Yard fault may act as a recharge zone, where the buried Paleozoic sedimentary rock aquifer is in hydro-logic communication with rift-filling sediments.

Aquifer Compartmentalization

Several of the intrabasin faults act as hydrologic boundaries, and result in some compartmentalization of the deep basin-fill aquifer. The Seco fault acts as an impermeable boundary, and may act to separate a northeast deeper aquifer system that has been recharged by modern to Holocene precipitation separated from a southwest deep aquifer system that has been recharged by older, possibly Pleistocene precipitation (Drakos et al., this volume). Data from high-precision temperature logs also indi-cates compartmentalization of the deep basin fill aquifer (Reiter and Sandoval, this volume). Some Los Cordovas fault splays act as impermeable boundaries (e.g. the eastern Los Cordovas fault near BOR1 and one or both of Los Cordovas faults near RP2500), whereas other faults do not appear to affect groundwater flow in the deep aquifer (e.g. the western Los Cordovas fault near the Airport well and near UNM/Taos). This may indicate variable cementation along the fault plane and/or variable offset along Los Cordovas fault strands.

Aquifer Anisotropy/Vertical Hydraulic Conductivity

Ojo Caliente Sandstone Member of Tesuque Formation

The RP2500/RP2000 and K3/K2 pumping test configurations included observation wells completed in both the Ojo Caliente

Well Name TD (ft) StaticDTW (ft)

Testlength(min)

Q (gpm) T (ft2/day) b (ft) K (ft/day) Storagecoefficient

Boundariesobserved Source Comments

UNM/Taos 1200 310 2737 60 670 200 3.4 GGI possibly Chamita Fm?

NGDOM 1400 266 5,760 140 760 400 1.9 n.a. impermeable GGI ddn observed in adjacent deep well (BOR1); no ddn in shallow completion

BOR1 2003 281 5,760 240 1400 (early) 520 (late)

510 1.9 n.a. impermeable GGI early-time k = 2.8 ft/day; late time k = 1.0 ft/day; drawdown observed in adjacent shallow well (NGDOM)

BOR2B 1480 83 2,880 67 280 480 0.6 n.a. none GGI no ddn in overlying or underlying aquifersBOR3 2109 274 15,840 500 710 (early)

450 (late)530 1.1 5 x 10-4 none/possible

facies changeGGI early-time k = 1.3 ft/day; late time k = 0.9

ft/day; no drawdown observed in overlying aquifers

TABLE 4. Aquifer testing data from wells completed in Chama-El Rito Member of Tesuque Formation, southern San Luis Basin. Well locations included in Appendix A.

HYDROLOGIC CHARACTERISTICS OF BASIN-FILL AQUIFERS

Appendix C page 12

402

and the overlying Agua Azul (Servilleta) aquifers. Drawdown was not observed in the overlying Agua Azul aquifer during 400 gpm, 10,000 to 12,000 min pumping tests. Without additional piezometers in the Chamita Formation sediments that overlie the Ojo Caliente, and with the presence of strong negative boundary effects observed in the pumping test data, K’ in the Ojo Caliente-Chamita Formation aquifer system cannot be evaluated. During the time frame of the pumping tests, no connection was observed between the shallow (Agua Azul) and deep (Ojo Caliente) aqui-fers.

Chama-El Rito Member of Tesuque Formation

The BOR1/NGDOM and BOR2/BOR3 pumping test con-figurations included observation wells completed in both the producing interval and water-bearing zones in the overlying Ter-tiary deposits and shallow alluvial aquifers. Drawdown was not observed in the overlying shallow alluvium during any of the five tests conducted on BOR1, NGDOM, BOR2B, BOR2C, or BOR3 (Table 4). Hydrologic communication was observed between BOR1 and NGDOM during pumping tests on each well, indi-cating leakage between different producing intervals within the Chama-El Rito aquifer at that location. However, it is notable that no drawdown was observed in BOR2B (bottom of screened inter-val = 1480 ft) during the 15,840 min (11 day), 500 gpm pumping test on BOR3 (top of screened interval = 1604 ft). BOR3/BOR2 test data indicate that clay beds with very low K’ are present within the Chama-El Rito Member at some locations. These pre-liminary data do not allow for a direct calculation of K’ but show that K’ likely varies significantly throughout the Chama-El Rito aquifer system. During the time frame of the pumping tests, no connection was observed between the Agua Azul or shallow allu-vial aquifers and the Chama-El Rito aquifer.

BASIN MARGIN AQUIFER

Hydrologic Characteristics of the Basin Margin Aquifer

Wells completed into fractured sedimentary and crystalline rock aquifers, while not utilized extensively for municipal use, are utilized for individual domestic and small community water systems. Where fractured, these aquifers are productive but likely are limited in areal extent and are subject to dewatering of the fracture system. In the southern part of the study area, the basin margin aquifer has a moderate to high gradient of 0.1 to 0.7 ft/ft to the northwest (Bauer et al., 1999). Water table elevation contours from Bauer et al. (1999, Plate 1) indicate that the basin margin aquifer discharges to the shallow basin fill aquifer.

Limited aquifer testing data are available from three wells completed into fractured Paleozoic sedimentary rocks or frac-tured crystalline rocks, two of which are located in basin margin settings (Figure 5; Table 5). Well depths range from 400 to 1200 ft (120 to 365 m) in depth, and include the Town Yard well, drilled into the Paleozoic Alamitos Formation underlying the Tertiary sediments in the southeast part of the study area (Fig. 4, Table 5). Pumping tests were run for times ranging from 435 to 2880 min at Q ranging from 8 to 48 gpm (Table 5). Based on these limited test results, the fractured sedimentary rock and crystalline rock aquifers exhibit hydraulic conductivity (K) ranging from 0.1 to 2.8 ft/day. Data on S are not available. Head in the Ruckendorfer and Yaravitz wells is at a similar elevation to the head in the shal-low alluvial aquifer (Fig. 5), indicating that these basin margin wells are discharging to the shallow alluvial aquifer

CONCLUSIONS

Two major aquifer systems are present in the Taos area. The shallow aquifer includes the Servilleta Formation and overlying alluvial deposits. The deeper aquifer includes Tertiary age rift-fill sediments below the Servilleta Formation. The shallow aqui-fer system includes unconsolidated alluvial fan and axial fluvial deposits overlying and interbedded with and including the Servil-leta basalts and is subdivided into: 1) unconfined alluvium; 2) leaky-confined alluvium, and; 3) the Servilleta Formation. The deep Tertiary basin-fill aquifer includes the Chamita Formation, the Ojo Caliente Sandstone Member of the Tesuque Formation, the Chama-El Rito Member of the Tesuque Formation, and the Picuris Formation.

Hydraulic conductivity in the shallow unconfined alluvial aquifer ranges from 6.8 ± 5.9 ft/day for the unconfined alluvial facies to 12.0 ± 8.6 ft/day for the Agua Azul aquifer facies. The deep leaky-confined alluvial wells exhibit K values ranging from 0.1 to 17.4 ft/day, and fall into two distinct populations and geo-graphic groupings. The low-K (mean K = 0.4 ft/day) deep aquifer facies corresponds to older Blueberry Hill mudflows or weath-ered fan deposits underlying the large Rio Hondo alluvial fan in the northern portion of the study area. The high-K (mean K = 11.4 ft/day) deep alluvial aquifer facies corresponds to young (?), less-weathered deposits underlying the small Rio Pueblo de Taos fan. A K’ of 0.2 ft/day was calculated from a single test in the alluvial aquifer, and a K’ of 0.02 ft/day through the USB was calculated from a single Agua Azul test. Storativity of the alluvial aquifer ranges from 10-4 to 10-2.

The deep basin-fill aquifer system is subdivided into the Chama-El Rito and Ojo Caliente facies. Ojo Caliente wells exhibit K of 0.4 ± 0.25 ft/day. S values for Ojo Caliente wells

Well Name TD (ft) StaticDTW (ft)

Testlength(min)

Q (gpm)ft2/day

b (ft) T (ft2/day) Storagecoefficient

Boundariesobserved Source Comments

Yaravitz 400 93 2880 31 310 110 2.8 n.a. none GGI fractured amphibolite/granite along faultTown Yard 1020 115 435 48 400 300 1.3 n.a. none GGI open hole test; preliminary data for Pz Ruckendorfer 600 391 2880 8 20 170 0.1 n.a. impermeable? GGI poor curve match; Pz sandstone aquifer

TABLE 5. Aquifer testing data from basin margin wells, southern San Luis Basin. Well locations included in Appendix A.

DRAKOS ET AL.

Appendix C page 13

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Bauer, P.W., and Kelson, K., 2004, Cenozoic structural development of the Taos area, New Mexico, in New Mexico Geological Society, 55th Field Confer-ence Guidebook, p. 129-146.

Cordell, L., 1978, Regional geophysical setting of the Rio Grande rift: Geological Society of America Bulletin 89, p. 1073-1090.

Drakos, P., Hodgins, M., Lazarus, J., and Riesterer, J., 2001, Subsurface stratigra-phy and Stratigraphic correlations from Taos deep drilling and groundwater exploration program (abs): New Mexico Geological Society Proceedings Volume, 2001 Annual Spring Meeting, p. 40.

Drakos, P., Lazarus, J., Riesterer, J., White, B., Banet C., Hodgins, M., and San-doval, J., 2004, Subsurface stratigraphy in the southern San Luis Basin, New Mexico in New Mexico Geological Society, 55th Field Conference Guide-book, p. 374-382.

Dungan, M.A., Muehlberger, W.R., Leininger, L., Peterson, C., McMillan, N.J., Gunn, G., Lindstrom, M., and Haskin, L., 1984, Volcanic and sedimentary stratigraphy of the Rio Grande gorge and the late Cenozoic geologic evolu-tion of the southern San Luis Valley, in New Mexico Geological Society Guidebook 35th Field Conference, Rio Grande Rift: Northern New Mexico, p. 157-170.

Galusha, T., and Blick, J., 1971, Stratigraphy of the Santa Fe Group, New Mexico: Bulletin of the American Museum of Natural History, v. 144, Article 1.

Hantush, M.S., and Jacob, C.E., 1955, Non-steady radial flow in an infinite leaky aquifer, Am.Geophys. Union Trans., vol., 36, p. 95-100.

Keller, G.R., and Cather, S.M., 1994, Introduction, in Keller, G.R., and Cather, S.M., eds., Basins of the Rio Grande Rift: Structure, Stratigraphy, and Tec-tonic Setting, Geological Society of America Special Paper 291, 1994, p. 1-3.

Kelson, K.I., and S.G. Wells, 1987, Present-day fluvial hydrology and long-term tributary adjustmens, northern New Mexico, in Menges, C., ed, Quaternary Tectonics, Landform Evolution, Soil Chronologies and Glacial Deposits – Northern Rio Grande Rift of New Mexico: Friends of the Pleistocene – Rocky Mountain Cell fieldtrip guidebook p. 95-109.

Kelson, K.I., and S.G. Wells, 1989, Geologic Influences on Fluvial Hydrology and Bedload Transport in Small Mountainous Watersheds, Northern New Mexico, USA; Earth Surface Processes and Landforms, vol. 14, p. 671-690.

Lipman, P.W., 1978, Antonito, Colorado, to Rio Grande gorge, New Mexico, in Hawley, J.W., Guidebook to Rio Grande rift in New Mexico and Colorado: New Mexico Bureau of Mines and Mineral Resources Circular 163, p. 36-42.

Machette, M., and Personius, S., 1984, Map of Quaternary and Pliocene faults in the eastern part of the Aztec 1° by 2° Quadrangle and the western part of the Raton 1° by 2° Quadrangle, northern New Mexico, USGS Miscellaneous Field Studies Map MF-1465-B, scale 1:250,000.

Reiter, M., and Sandoval, J., 2004, Subsurface temperature logs in the vicinity of Taos, New Mexico, in New Mexico Geological Society, 55th Field Confer-ence, p. 415-419.

Sanford, A.R., Balch, R.S., and Lin, K.W., 1995, A Seismic Anomaly in the Rio Grande Rift Near Socorro, New Mexico, New Mexico Institute of Mining and Technology Geophysics Open File Report 78, 18 p.

Spiegel, Z., and Couse, J.W., 1969, Availability of ground water for supplemental irrigation and municipal-industrial uses in the Taos Unit of the U.S. Bureau of Reclamation San Juan-Chama Project, Taos County, New Mexico: New Mexico State Engineer, Open-File Report, 22 p.

Wells, S.G., Kelson, K.I., and Menges, C.M., 1987, Quaternary evolution of fluvial systems in the northern Rio Grande Rift New Mexico and Colorado: Impli-cations for entrenchment and integration of drainage systems, in Menges, C., ed, Quaternary Tectonics, Landform Evolution, Soil Chronologies and Glacial Deposits – Northern Rio Grande Rift of New Mexico: Friends of the Pleistocene – Rocky Mountain Cell fieldtrip guidebook p. 55-69.

range from 10-3 to 10-2. Chama-El Rito wells exhibit a K of 1.8 ± 1.0 ft/day. An S of 5 x 10-4 was calculated from the BOR3/BOR2 pumping test.

Faults typically do not act as impermeable boundaries in the shallow alluvial aquifer. However, the Seco fault and several of the Los Cordovas faults act as impermeable boundaries in deep basin-fill aquifer. The Town Yard fault is a zone of enhanced permeability or is coincident with a high-permeability zone in the shallow alluvial aquifer, and does not act as an impermeable boundary in the deep basin fill aquifer. Intrabasin faults with sig-nificant offset, such as the Seco fault, result in compartmentaliza-tion of the aquifer.

Groundwater flow direction in the composite Alluvial plus Servilleta aquifer system is from northeast to southwest and from east to west at 0.02 ft/ft. A broad groundwater trough is observed whose axis is north of Rio Pueblo de Taos and west of Rio Lucero This trough may correspond to an area of high-permeability flu-vial deposits associated with the ancestral Rio Hondo, whose course was controlled by the Rio Pueblo de Taos syncline. An area exhibiting a downward vertical gradient in the shallow aqui-fer is observed between the Rio Hondo and Rio Lucero in the northern part of the study area. The limited available data suggest that groundwater flow direction in the deep aquifer is generally from east to west, at a relatively shallow gradient of approxi-mately 0.004 ft/ft. Downward gradients are observed in the deep basin-fill aquifer except at the Rio Pueblo de Taos syncline, where upward gradients are observed at RP2500/RP2000 and K2/K3.

ACKNOWLEDGMENTS

The authors would like to acknowledge contributions to this effort by the following individuals or agencies. Gustavo Cordova and Tomás Benavidez from the Town of Taos and Nelson Cor-dova and Gil Suazo of Taos Pueblo provided impetus and support for the design and implementation of the deep drilling program and promoted an open exchange of technical data. The US Bureau of Reclamation provided funding under the direction of John Peterson for the deep drilling and testing program. Mark Lesh of Glorieta Geoscience, Inc. produced the figures, and Mustafa Chudnoff provided helpful review comments. Dr. Paul Bauer and Keith Kelson provided helpful discussions on the aquifer ana-logs. Dr. John Shomaker, Dr. John Hawley, and Dr. Brian Brister provided critical reviews of the manuscript.

REFERENCES

Bauer, P., Johnson, P. and Kelson, K., 1999, Geology and hydrogeology of the southern Taos Valley, Taos County, New Mexico: Final Technical Report, New Mexico Bureau of Mines and Mineral Resources, 56 p. plus plates.

HYDROLOGIC CHARACTERISTICS OF BASIN-FILL AQUIFERS

Appendix C page 14

404

APPENDIX A

WELL LOCATIONS FOR TAOS AREA WELLS CITED IN THIS STUDY

UTM NAD 27, zone 13, m. UTM NAD 27, zone 13, m.WELL NAME Easting Northing WELL NAME Easting NorthingAbeyta Well 448752 4024118 Howell 448470 4030712

Arroyo Hondo 452696 4046154 K2 - K3 446688 4030429Arroyo Park 443740 4028440 Kit Carson 448900 4029260Arroyo Seco 448745 4041260 La Percha 445760 4030300

Arroyos del Norte 446162 4042084 Landfill MW1 442758 4034011Baranca del Pueblo 437160 4023520 Lerman 441824 4032655

Bear Stew 450352 4037199 Mariposa Ranch 445180 4040820BIA 11 444775 4035824 McCarthy 446307 4038831BIA 13 448320 4034830 Mesa Encantada 442346 4024531BIA 13 449820 4029780 NGDOM 442290 4022740BIA 14 449470 4030990 OW-6 449590 4033200BIA 15 442470 4028200 Pettit Well 447925 4023423BIA 17 448890 4038130 Porter 447769 4041305BIA 2 449600 4033180 Quail Ridge 446472 4035777

BIA 20 447335 4035901 Ranchos Elem. Sch 446316 4023297BIA 24 447500 4038340 R. Fernando de Taos 450851 4025541BIA 9 444280 4038930 R.G. del Rancho 447172 4020228

BJV #1 441230 4023480 Rio Lucero 448028 4030617BOR 1 442124 4022604 R. Pueblo de Taos 448731 4030516

BOR 4 Deep 444766 4035805 Riverbend 439120 4024530BOR 6 #1 444797 4035805 Rose Gardiner 443027 4024817BOR 6 #2 444797 4035805 RP 2000 Deep 440380 4026000BOR2A 446247 4026541 RP 2500 440462 4026069

BOR2B/2C 446240 4026553 Ruckendorfer 449460 4023920BOR3 446247 4026541 Taos SJC 440340 4026080BOR5 447345 4035906 TOT #1 448626 4029394BOR7 444280 4038930 TOT #2 448648 4029400

Cameron 446529 4034294 TOT #3 448941 4029690Cielo Azul 446420 4040260 TOT #5 448631 4028835

Cielo Azul Deep 446400 4040250 Town Taos Airport 439480 4034760Colonias Point 444910 4034920 Town Yard 447060 4026680

Cooper 443860 4029120 UNM/Taos 441310 4022260Fred Baca Park 447225 4028617 Vista del Valle 443681 4023916

Hank Saxe 440507 4020477 Yaravitz 449826 4042805

DRAKOS ET AL.

Appendix C page 15